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BUREAU OF GEOLOGY 


C. W. SHANNON, DIRECTOR 
F. M. BULLARD, CHIEF GEOLOGIST 


BULLETIN NO. 2 


GEOLOGY OF THE STONEWALL QUADRANGLE, 
OKLAHOMA 

BY 

GEO. D. MORGAN 





NORMAN 
January, 1924 






Qt'M 

1^24 


COPYRIGHT, 1924 
BY 

BUREAU OF GEOLOGY 
All rights reserved 


may 22 


m 


©C1A792354) 




GEOLOGY OF THE STONEWALL QUADRANGLE, 

OKLAHOMA 


CONTENTS 


Location- 1 3 

Acknowledgments - 1 3 

Introduction- 1 7 

General and historical geology- 17 

Stratigraphy- 21 

Arbuckle limestone--- 21 

Name - 21 

Areal distribution- 21 

Thickness and character-- 22 

Fossils ---— 2 3 

Age and correlation- 23 

Structure- 24 

Economic importance-- 2 3 

Simpson formation- 2 3 

Name - 2 3 

Areal distribution- 2 3 

Thickness and character- 26 

Fossils - 27 

Age and correlation- 30 

Structure- 30 

Economic importance- 30 

Viola limestone- 30 

Name - 30 

Areal distribution- 31 

Thickness and character- 31 

Fossils - 32 

Age and correlation- 33 

Structure - 34 

Economic importance-- 34 

Sylvan shale--- 34 

Name- 34 

Areal distribution- 34 

Thickness and character- 35 






































4 


CONTENTS 


Fossils _ 3 5 

Age and correlation_ 3 6 

Economic importance_ 36 

Hunton terrane- 36 

Name _ 36 

Areal distribution_ 36 

Thickness and character_ 3 7 

Divisions _ 3 7 

Chimneyhill limestone_ 3 7 

Description _ 3 7 

Fossils _ 39 

Oolitic member_ 39 

Glauconitic member_ 39 

Pink crinoidal member_ 39 

Henryhouse shale_ 39 

Description - 39 

Fossils _ 39 

Lower Henryhouse- 40 

Upper Henryhouse_ 40 

Haragan shale- 40 

Description - 40 

Fossils _ -40 

Bois d’Arc limestone- 41 

Description_ 41 

Fossils _ 42 

Structure- 42 

Economic importance_ 42 

Woodford formation_ 42 

Name _ 42 

Areal distribution_ 43 

Thickness and character_ 44 

Fossils _ 45 

Age and correlation_ 46 

Structure _ 48 

Economic importance_ 48 

Sycamore limestone_ 48 

Name _ 48 

Areal distribution- 48 

Thickness and character_ 49 

Fossils _ 50 

Age and correlation- 50 

Caney shale- 50 

Name - 50 

Areal distribution _ 51 * 

Thickness and character- 53 















































CONTENTS 


5 


Fossils _ 53 

Age and correlation_ 56 

Structure _ 56 

Wapanucka formation___ 56 

Name _ 56 

Areal distribution_ 56 

Thickness and character_ 5 7 

Fossils _ 60 

Age and correlation_ 60 

Structure _ 60 

Economic importance_ 60 

Atoka formation _ 62 

Name _ 62 

Areal distribution _ 63 

Thickness and character_ 63 

Fossils _ 64 

Age and correlation_ 65 

Structure _ 65 

Economic importance__ 65 

Hartshorne sandstone_:_ 65 

Name _ 65 

Areal distribution_ 65 

Thickness and character_ 66 

Fossils _ 66 

Age and correlation_ 66 

Structure -_ 67 

Economic importance_ 67 

McAlester formation_ 67 

Name - 67 

Areal distribution-*_ 67 

Thickness and character_ 67 

Fossils _ 70 

Age and correlation- 71 

Structure _ 71 

Economic importance- 74 

Savanna sandstone- 74 

Name - 74 

Areal distribution- 74 

Thickness and character_ 74 

Jolly limestone member- 74 

Fossils _ 77 

Age and correlation_ 7 7 

Structure - 77 

Economic importance - 77 

Boggy formation- 7 7 















































6 


CONTENTS 


Name _ 7 7 

Areal distribution_ 7 7 

Thickness and character_ 77 

Fossils - 80 

Age and correlation_ 80 

Structure - 80 

Economic importance_ 84 

Thurman sandstone_ 84 

Name _ 84 

Areal distribution _ 84 

Thickness and character_ 84 

Fossils _ 85 

Age and correlation_ 85 

Structure _ 85 

Stuart shale- 85 

Name _ 85 

Areal distribution_ 85 

Thickness and character_ 86 

Fossils _ 86 

Age and correlation_ 86 

Structure _ 86 

Senora formation_ 86 

Name _ 86 

Areal distribution_ 86 

Thickness and character- 87 

Fossils _ 87 

Age and correlation- 87 

Structure- 87 

Calvin sandstone- 89 

Name - 89 

Areal distribution_ 89 

Thickness and character_ 89 

Fossils _ 90 

Age and correlation_ 90 

Wetumka shale - 91 

Name ___ 91 

Areal distribution_ 91 

Thickness and character_ 91 

Fossils _ 91 

Age and correlation_ 91 

Structure - 93 

Wewoka formation ___ 93 

Name _ 93 

Areal distribution_ 93 

Thickness and character_ 94 















































CONTENTS 


7 


Fossils _ 101 

Age and correlation_ 101 

Structure_101 

Holdenville formation _ 101 

Name - 101 

Areal distribution_ 101 

Thickness and character_ 103 

Sasakwa limestone member_ 103 

Homer limestone member_ 104 

Fossils _ 105 

Age and correlation_ 105 

Structure _ 105 

Seminole formation_ 109 

Name _ 109 

Areal distribution_ 109 

Thickness and character___ 109 

DeNay limestone_ 110 

Fossils _ 112 

Age and correlation_ 112 

Structure_ 112 

Francis formation_ 113 

Name _ 113 

Areal distribution _ 113 

Thickness and character- 11 4 

Fossils ___ 11 5 

Age and correlation- 115 

Structure _ il5 

Economic importance - 1 1 9 

Franks conglomerate- 119 

Name - 119 

Areal distribution- 1 1 9 

Thickness and character- 119 

Age and correlation- 120 

Conglomerates at Sulphur- 121 

Possibility of correlating conglomerates at Sulphur with the 

Seminole conglomerate- 122 

Conclusions- 122 

Belle City limestone- - - 123 

Name _ 123 

Areal distribution- 123 

Thickness and character- 123 

Fossils - 125 

Age and correlation- 125 

Structure - 125 

Vamoosa formation- 125 

0 * 














































CONTENTS 


i 


Name _ 125 

Areal distribution - 125 

Thickness and character_ 125 

Age and correlation_ 126 

Structure _ 128 

Ada formation_ 128 

Name _ 128 

Areal distribution_ 128 

Thickness and character_ 128 

Fossils _ 131 

Age and correlation_ 132 

Structure - 132 

Economic importance_ 132 

Pontotoc terrane_ 132 

Name _ 132 

Areal distribution and character- 132 

Divisions _133 

Vanoss formation_ 133 

Name _ 133 

Thickness and character_ 133 

Age and correlation_ 134 

Stratford formation_ 137 

Name _ 137 

Thickness and character_ 137 

Fossils _ 139 

Age- 139 

Konawa formation_ 140 

Name _ 1 40 

Areal distribution_ 140 

Thickness and character_ 140 

Age - 141 

Asher formation _ 141 

Name - 141 

Thickness and character- 142 

Age- 142 

Guertie sand_ 142 

Name _ 142 

Character and distribution___ 142 

Fossils _ 144 

Age_ 145 

Structure - 145 

Economic importance _ 145 

River sand_ 145 

Structure - 145 

General statement_ 145 















































CONTENTS 


9 


Northwestern area_146 

General structure_ 146 

Sasakwa anticline and fault_ 146 

Anticline in the western edge of T. 6 N., R. 7 E_147 

West end of Allen anticline_ 147 

Fold in the northwest corner of T. 4 N., R. 8 E._148 

Beebe anticline_ 148 

Fold southeast of Maxwell_ 148 

Fold west of Oakman_i_ 148 

Fault block northeast of Byng_149 

Structure of the Ada gas field_ 149 

Center anticline_ 149 

Syncline south of Vanoss___ ISO 

Steep-dip zone in T. 3 N., R. 5 E_ 150 

Southeastern area_,_150 

General structure __ 150 

Lawrence uplift_ l5o 

Ahlosa fault- 151 

Stonewall fault- 15 1 

Minor folding_ 152 

Franks graben_ 153 

Structure of the Arbuckle Mountains proper-15 5 

Subsurface structure- 156 

Correlations-15 6 

Well logs- 158 

Paleontology - 174 

General statement_ 1 74 

Faunal charts- 174 

Description of new species-174 

Anthozoa - 174 

Bryozoa _ 176 

Brachiopoda__ 184 

Pelecypoda- 184 

Cephalopoda - 185 

Description of plates- 187 -238 

Register of localities_ 239 

References--246 







































10 


ILLUSTRATIONS 


ILLUSTRATIONS 


Page 

Index Map --- *6 

Plate I. Geologic map of the Stonewall quadrangle-In pocket 

II. Reconstructed section, Oklahoma to Canada, at the close 

of the Ordovician- l 7 

III. Columnar section, Stonewall quadrangle, Oklahoma- 18 

IV. Geologic cross-section_ 20 

V. A cross-bedded, conglomeratic sandstone in the upper 
part of the Arbuckle limestone in sec. 29, T. l N., 

R. 7. E._ 24 

VI. Northward dipping Simpson strata in glass-sand pit north 

of the town of Hickory_ 29 

VII. Structural map. Top of Hunton terrane is datum plane__ 43 

VIII. Bluff of Woodford formation on Goose Creek. Location 

in northeast quarter of sec. 26, T. 1 N., R. 7 E._ 45 

IX. McAlester-Caney contact on south bank of Sheep Creek. 

Location near the center of sec. 1, T. 1 N., R. 6 E. 

Note the thin bed of conglomerate along the con¬ 
tact - 51 

X. A. Lehigh coal bed as exposed in the strip pit in sec. 14, T. 

1 N., R. 7 E.- 68 

B. General view of strip pit in sec. 14, T. 1 N., R. 7 E_ 69 

XL Thin-bedded Calvin sandstone in northeast corner sec. 36, 

T. 4 N., R. 7 E._ 90 

XII. A. Limestone conglomerate in the Wewoka formation, in the 

southeast corner, sec. 11, T. 3 N., R. 6 E_ 95 

XII. B. Cross-bedded sandstone in the Wewoka formation, in sec. 


95 















ILLUSTRATIONS 


11 


Sandstone member at the top of the Wewoka formation. 

Top of eastward-facing escarpment, in the northeast 
quarter of sec. 16, T. 3 N., R. 6 E. Below this mem¬ 
ber is about IS feet of Wewoka shale which rests un- 
conformably on the Boggy formation_ 96 

Sasakwa limestone member of the Holdenville formation 

exposed in quarry one-fourth mile south of Sasakwa 103 


XV. A. Massive chert conglomerate, at the base of the Seminole 
formation. Location in the northeast quarter of sec. 

18, T. 6 N., R. 8 E. This is the type area of the 
Seminole _ill 

B. Local unconformity between the Seminole and Holdenville 
formations. Location in the northeast quarter of 
sec. 18, T. 6 N., R. 8 E. This is the only locality at 
which an unconformity between the two formations 
was observed_ ill 


XVI. A. Detail of massive chert conglomerate, characteristic of a 

large part of the Vamoosa formation_127 

B. General view of chert conglomerate in the upper part of 

the Vamoosa formation in sec. 26, T. 6 N., R. 6 E_127 


XVII. A. Limestone conglomerate in the Ada formation, one-half 

mile west of Ada- 130 

B. Asphaltic sandstone in the Ada formation. Location, as¬ 
phalt pit one mile west of Ada_130 

XVIII. Apparatus used in washing asphaltic sands of the Simpson 

formation-‘- 131 

XIX. A. Massive, arkosic sandstone in the Vanoss formation, in 

sec. 29, T. 6 N., R. 6 E._135 

B. Limestone conglomerate in the Vanoss formation, one mile 
east of Sulphur. This bed carries a small amount of 
arkosic material - 135 


XX. Arkosic limestone—the Hart limestone member of the 
Stratford formation. Location, west-central part of 
section 4, one and one-half miles west of Vanoss. 

Note the large size of the feldspar crystals embedded 
in the limestone-----138 

XXL Massive chert conglomerate in the Konawa formation. 

Location, on main road 3 miles east of Asher. 

In common with most of the strata of this formation 
the beds here exposed are slightly arkosic- 140 













12 


ILLUSTRATIONS 


XXII. A. Elephant tusk in Guertie sand near center of south line, 

sec. 10, T. 3 N., R. 5 E.___143 

B. Guertie sand, one-half mile north of Byng_143 

XXIII. Mastodon tooth found at Red Springs, southeast of Steed- 

man, Okla._ 144 

XXIV. Structural map of the Stonewall quadrangle-In pocket 

XXV. Geologic and structure sections-In pocket 

XXVI. Offset fault in Holdenville formation. Location northeast 
quarter, section 34, T. 2 N., R. 6 E., just north of 
the Hunton fault blocks described by Reeds. Picture 
taken looking west- 154 

XXVII. Correlation table_ 15 7 

XXVIII. Faunal chart_In pocket 

XXIX.-LIII. Fossil plates_187 - 237 


Figure I. 


Cross-section through sections 3 and 10, T. 3 N., R 7 E.__79 











TAMILS 


TABLES 


Correlation table of the Siluro-Devonian rocks, Arbuckle Mountains, 

Oklahoma_ 38 

Range and distribution of species in the Woodford formation_ 4 7 

Fauna of the Caney shale-5 4 and 55 

Fauna of the Wapanucka formation-61 and 62 

Fauna of the McAlester formation_72 and 73 

Fauna of the Savanna formation- 76 

Fauna of the Boggy formation-81 - 83 

Fauna of the Senora formation- 88 

Fauna of the Wetumka shale- 92 

Fauna of the Wewoka formation___97 - 100 

Fauna of the Holdenville formation-106 - 108 

Fauna of the Seminole formation- 113 

Fauna of the Francis formation- 116- 118 

Fauna of the Belle City limestone-124 




















GEOLOGY OF THE STONEWALL QUADRANGLE, 
OKLAHOMA 


Published by permission of the Empire Gas and Fuel Company. 


LOCATION 

The Stonewall quadrangle is located in southern Oklahoma, 
along the northern flank of the Arbuckle Mountains. The quad¬ 
rangle embraces most of Pontotoc County and portions of McClain, 
Garvin, Murray, Johnston, Coal, Hughes, Seminole, and Potta¬ 
watomie counties. 

The United States Geological Survey has published folios on 
the Coalgate quadrangle to the east, the Atoka quadrangle to the 
southeast, and the Tishomingo quadrangle to the south of the 
Stonewall. 


ACKNOWLEDGMENTS 

Assistance in the preparation of the paper here submitted has 
been derived from many sources. Most of the expense was borne 
by the Empire Gas and Fuel Company, although some cooperation 
and financial support were received from the Oklahoma Geological 
Survey and the Bureau of Geology. The writer is deeply indebted to 
Dr. L. C. Snider, Chief Geologist for the Empire Companies and to 
Mr. C. W. Shannon, Director of the Bureau of Geology, both of 
whom contributed valuable suggestions regarding the work. Especial 
acknowledgments are due Mr. A. E. Brainerd who ably assisted in 
most of the field investigation. Messrs. Donald G. Barnett and 
Wm. J. Stahl did the instrument work, and Mr. Frank Ghartz did 
most of the drafting on the geologic maps, and Mrs. Bess Mills Bul¬ 
lard did the drafting of the structural maps, sections, and charts. 

Sincere appreciation is expressed ,to the members of the De¬ 
partment of Geology at Columbia University under whose super¬ 
vision and direction the manuscript was prepared. Professor J. J. 
Galloway, in charge of the stratigraphic work at Columbia, gave 
especial assistance as did Dr. H. N. Coryell, who is responsible for 
the identifcation of the Bryozoa, and Mr. Howard Meyerhoff, who 
helped prepare the plates. Professor Charles Schuchert of Yale Uni¬ 
versity spent several days in the field with the writer and has given 




16 


INDEX MAP 



Areq of published Folios of the U S. 
Geological Survey. 




































Bl AU OF GEOLOGY 


BULLETIN 2 PLATE II 




- 


Oklahoma 


Arkansas MissourHIlinois II linois’lowa Wisconsin'Minneso+a 


. A 'laysvl/lt t 




-Viola 




-PJaff-in i 7T 







y. 

x A x x x x * ~ x 
X * *x*x*x 

y. Gombrian * 

* * y. > 

* * X * ** * * 

X X X y. y. X > 

X v * > * X ^ v 



f'V PreGamkirian * * * * 

* * * * X X X ^ > Tfc ''X 

* + + * » * * * * * , „ * « * % 

* * + * * * * » ^ ‘ * * * 

* ■+■ * X X X X X 

+ + + * * -* * * * * * x * * * X * 


^ V- X 

X X * X XX 


X. 


x x 


RECONSTRUCTED SECTION, OKLAHOMA TO CANADA, AT THE CLOSE OF THE ORDOVICIAN. 
After C. L. Dake, University of Missouri Bulletin, vol. 6, No. 1, 1921 



















































































































































































































































GENERAL AND HISTORICAL GEOLOGY 


17 


many valuable suggestions. Mr. David White of the United States 
Geological Survey, is largely responsible for the identification of the 
plant fossils. 

Several earlier publications have been drawn upon, the authors 
of these receiving credit in the text. 

INTRODUCTION 

Although the title of the present paper is “Geology of the 
Stonewall Quadrangle” but little has been contributed to the 
knowledge of formations below the Woodford. For the sake of 
completeness, summarized discussions of the older formations are 
given and some newly discovered facts are included. A few chang¬ 
es have been made in the mapping, but, in the main, the maps and 
conclusions by Taff and Reeds for the formations that are exposed 
in the south central part of the area are accepted. 

Eighteen months were spent in the field investigation, the 
greater part of which was devoted to the “Carboniferous” strata. 
An areal map of the quadrangle has been prepared, the fauna and 
flora of all formations above the Hunton terrane were collected and 
studied, and a structural map, based on plane table surveys, was 
constructed for most of the area. 

The main contributions of this work may be summarized as 
follows: 

1. The areal and structural maps involving a determination 
of the rather complicated stratigraphic relations. 

2. The presentation of the fauna and flora of the strata above 
the Hunton terrane. 

3. Suggestions as to the periods at which the area was sub¬ 
jected to folding and faulting. 

GENERAL AND HISTORICAL GEOLOGY 

The strata exposed in the Stonewall quadrangle range in age 
from upper Cambrian to Recent. As might be expected, however, 
the section is incomplete. Several systems are entirely absent and 
there are large breaks in most of the others. 

Because of variation, both as to number and thickness, of the 
formations in the stratigraphic column at different parts of the area, 
it is difficult to estimate the average total thickness of sediments in 
the quadrangle. At the south end of the Arbuckle limestone out¬ 
crop, in the south-central part of the area, there are less than 4,000 
feet of strata; in the region just south of Stonewall the total thick¬ 
ness of the column is probably between 12,000 and 15,000 feet; 
and in that portion of the quadrangle which lies north of the Law- 


18 


GENERAL AND HISTORICAL GEOLOGY 


rence uplift there is an average thickness of about 10,000 feet of 
sediments. In the latter area the section is probably thinnest in the 
region of the Center anticline. The complete columnar section is 
given in Plate III. 

In general the sediments become more clastic toward the top 
of the section; in general also, they become coarser toward the 
Arbuckle and Ouachita mountains. The formations below the top 
of the Hunton terrane are predominantly of limestone; the succeed¬ 
ing Woodford and Caney formations are largely composed of black 
shale; the Wapanucka limestone, although shaley at the base, car¬ 
ries limestone in its upper portion; but succeeding formations are 
of shales, sandstones, and conglomerates with very little limestone. 

The structure of the area is complex and is evidently the re¬ 
sult of numerous movements that were quite variable both as to 
type and point of origin. 

The present structure of the Stonewall quadrangle is discussed 
in a later chapter. The movements which resulted in the structure 
may be summarized as follows: 

1. Slight warping movements initiated in the Arbuckle area 
at an early date, possibly in the late Cambrian or early Ordovician 
period. 

2. Warping and slight oscillation continued through Ordo¬ 
vician time. 

3. In early Silurian time arching movements in the Arbuckle 
area became more decided and the Arbuckle axis was defined. 

4. Magnitude of periodic arching movements increased during 
the Devonian and Mississippian so that by Pottsville time the Hunton 
and possibly Viola, Simpson, and Arbuckle formations were exposed 
near the southeast end of the present mountains. 

The crustal movements of these four periods were not persis¬ 
tently upward, throughout the area of the Stonewall quadrangle, as is 
indicated by the fact that during the time at which they were going 
on there were deposited in the Arbuckle area between 7,000 and 
10,000 feet of sediments. It is probable that the movements dur¬ 
ing the Cambrian and Ordovician were very slight and irregular, and 
that during the time at which they were going on there was a grad¬ 
ual increase in the relief between the bottom of the Arbuckle basin 
and the surface of adjoining land masses. This relative vertical 
divergence (whether caused by sinking of the basin, up¬ 
lift of the adjoining land areas, or by both processes) also continued 
through the Silurian and Devonian periods, but after the movements 
became decidedly positive with the resulting establishment of the 
Arbuckle axis, the axial area was probably more persistently above 
than below sea level. 




























































































































































































































































































































































































































































































































































GENERAL AND HISTORICAL GEOLOGY 


19 


5. Near the close of Atoka time .there was uplift followed by 
peneplanation and subsequent overlapping deposition of the Hart- 
shorne, McAlester, and at least part of the Savanna formations. 

6. Toward the close of Savanna time the Stonewall quad¬ 
rangle was subjected to a period of uplift and block faulting which 
resulted in the emergence of all the area with the possible excep¬ 
tion of the Franks graben. Peneplanation of the uplifted area 
followed and all formations down to the Wapanucka and Caney 
formations were stripped off of it. The eastern part of the Franks 
graben, near the quadrangle line, was near or below base level dur¬ 
ing this time and was unaffected by erosion. Following this period 
of peneplanation the Boggy shale and later formations, to near the 
top of the Wewoka, were then laid down unconformably on the 
peneplaned surface and across the Franks graben. That a part of 
the Arbuckle axis remained above sea level during all the time from 
Wapanucka to near the close of the Wewoka is indicated by the 
fragments of Caney, Woodford, Hunton, and Viola formations that 
are contained in the strata of the Wapanucka to late Wewoka for¬ 
mations inclusive. 

Progressive northward thrusting of the Ouachita area was ini¬ 
tiated near the beginning of Devonian time, and it is probable that 
this area contributed largely to all the sediments of the Stonewall 
quadrangle that lie between the base of the Woodford and the top 
of the Vamoosa formations. 

From Devonian time gradual uplift characterized the Arbuckle 
axis, and at the present time the older strata exposed there have a 
northward inclination that amounts to nearly 4,000 feet from the 
southern edge of the quadrangle to near its center. 

7. A little before the close of Wewoka time the Ouachita area 
was strongly uplifted. This movement resulted in the Choctaw 
fault which borders that area; it caused a general northwestward 
tilting of all the Pennsylvanian strata of the Coalgate and Stonewall 
quadrangles, and was accompanied by some faulting in the latter 
area. The fault along the northern side of the Lawrence uplift 
was formed at this time and the one along the southern side was 
renewed so that the intervening area was lifted high above the 
surrounding region. The uplift of the Lawrence block was dif¬ 
ferential, being greatest toward the west. This general period of 
uplift and faulting was followed by peneplanation, which at the 
western or highest part of the Lawrence uplift stripped off all the 
beds down to the lower part of the Boggy formation, and in the 
western end of the Franks graben removed all strata down to near 
the top of the Boggy. On the less uplifted eastern portion of the 
Lawrence area, in the low lying region to the north of this area, and 


20 


GENERAL AND HISTORICAL GEOLOGY 


in the eastern part of the Franks graben peneplanation was only 
slightly effective. 

The period of erosion was followed by transgression of the 
sea and the late Wewoka beds (about 30 feet thick) and subsequent 
strata, including the Vamoosa formation, were laid down. At the 
western end of the Lawrence uplift the Wewoka strata were de¬ 
posited on the eroded edges of lower Boggy beds, and in the west¬ 
ern end of the Franks graben the upper part of the Wewoka was laid 
down, probably on upper Boggy strata. Throughout all this period 
of deposition a great deal of angular chert conglomerate was 
brought into the Stonewall quadrangle. This type of sediment also 
characterizes the formations eastward toward the Ouachita Mountains 
and is thought to have been derived from that region. Portions 
of the Arbuckle axis were maintained above sea level during this 
period of deposition as is indicated by the limestone conglomerates 
in the Wewoka, Holdenville, and Francis formations, especially in 
their outcrops over the area of the Franks graben. 

8. Near the close of Vamoosa time there was an unusual up¬ 
lift of the Arbuckle axis that affected all the area embraced in the 
Stonewall quadrangle. The uplift resulted in slight renewal of 
movements along the already established fault lines and formed 
several new ones. The flexing and slight faulting of the late 
Wewoka, Holdenville, Seminole, and Francis formations along the 
northern side of the Lawrence uplift occurred at this time. The 
block faults that cut the Hunton and overlapping Holdenville forma¬ 
tions in the northwest quarter of section 34, west of Franks, were 
probably also caused by this movement as were the block faults east 
of Byng. 

The first result of this uplift was the peneplanation of much of 
the Stonewall quadrangle. This was followed by unconfprmable 
deposition, over most of the area, of a mantle of clastic sediments, 
largely composed of limestone conglomerates (Ada formation). 
The source of the conglomerates was the Arbuckle Mountains. 

The removal of this large amount of material from: the Ar- 
buckles exposed the granite core of the Mountains which thereafter, 
to the close of Pontotoc time, contributed an abundance of Arkosic 
material to the formations being deposited in the Stonewall quad¬ 
rangle. After the granite of the Arbuckles was exposed it apparent¬ 
ly eroded faster than did the bordering limestone to the north so 
that near the time at which the sandstone at the base of the Asher 
formation was deposited the granite surface had been reduced below 
the level of the bordering limestone. The granite then no longer 
contributed arkosic material to the sediments that were being laid 
down to the north of the Mountains. 


BUREAU OF GEOLOGY 


BULLETIN 2 PLATE IV 




































































STRATIGRAPHY 


21 


The uplift at the close of deposition of the Vamoosa forma¬ 
tion, and the subsequent peneplanation of the area occurred in late 
Pennsylvanian time. The Permian period began during the sub¬ 
sequent time of deposition. The base of the Permian system is 
placed at the bottom of the Hart limestone member of the Stratford 
formation and, northeastward from the point at which that member 
is thought to be overlapped, at the base of the Konawa formation. 

9. All of the Permian formations of the Stonewall quadrangle 
have been slightly folded indicating movements in the area during 
or subsequent to that period. 

Mesozoic and Tertiary strata are not represented in the Stone¬ 
wall quadrangle. 

During the Pleistocene the Guertie sand was laid down, prob¬ 
ably as a river deposit. 

In Recent time a thick sand deposit has been laid down in the 
Valley of Canadian River. 

STRATIGRAPHY 

ARBUCKLE LIMESTONE 

NAME 

The Arbuckle limestone composes the major portion of the 
central mass of the Arbuckle Mountains. No single type section 
was given by Taff 1 who named it, the name being derived from the 
Arbuckle Mountains as a whole. 

In the Tishomingo and Atoka quadrangles, to the south and 
southeast of the Stonewall quadrangle, the formation lies on the 
Reagan sandstone. In the latter area, however, it is the lowest 
formation exposed. 

AREAL DISTRIBUTION. 

In the Stonewall quadrangle the Arbuckle outcrop resembles 
in shape a broad northward-pointing wedge, the base of which ex¬ 
tends for some 16 miles along the southern edge of the area. 
The point of this wedge lies about 10 miles north of its base and is 
in the western part of T. 2 N., R. 5 E., a little more than a mile east 
of Roff. The outcrop here described is the only exposure of the 
Arbuckle within the quadrangle, but the formation is thought to have 
been encountered in the following wells at the depths listed: 

SE. sec., 11 T. N., R. 3 E-1,439 feet 

Town of Roff, sec., 24, T. 2 N., R. 4 E-1,000 feet. 

The areal extent of the formation is approximately 90 square 

1 Taff, J. A., U. S. Geol. Survey, Geol. Atlas, Atoka folio No. 79, 1903. 




22 


ARBUCKLE LIMESTONE 


miles, but notwithstanding the large size of this outcrop the lower 
portion of the formation is nowhere exposed within the limits of the 
area here considered. 

THICKNESS AND CHARACTER 

In his original 2 and subsequent 3 publications, dealing with the 
Arbuckle limestone, Taff assigns to it a thickness of between 4,000 
and 6,000 feet. This is the thickness also given by Reeds 4 and 
Howell 5 in more recent publications. 

Taff’s complete section of the formation, as measured in the 
Tishomingo quadrangle, beginning at the top, is as follows: 


Section of the Arbuckle limestone after Taff. 


Feet 

Medium and thin-bedded limestones _450 

These strata are associated with shaly strata, and, very 
near the top, with occasional sandy beds. 

Massive compact magnesian limestone _3,500-4,000 


The lower half of this portion contains chert in some 
portions. On weathering the limestones usually present 
smooth white surfaces of practically the same color as the 
fresh rock. 

Thin-bedded granular limestone and compact blue 

limestone _250 

Heavy-bedded dull-bluish and cream colored dolomites_300-400 
Many of these strata are very irregularly bedded and 
weather into brown or nearly black bowlders. Others are 
more crystalline, marble-like, and of pinkish or gray 
colors. 

Thin-bedded siliceous limestone- 50 

In the northwest corner of sec. 25, T. 1 N., R. 6 E., near the 
top of the formation, is a thin chert conglomerate which carries peb¬ 
bles up to three inches in length. Most of the pebbles are angular, 
but a few appear to be waterworn. A cross-bedded, conglomeratic 
sandstone (Plate V) was also observed in the north central part 
of sec 29, T. 1 N., R. 7 E. The pebbles here contained are mostly 
chert and sandstone, and ordinarily are not more than two inches in 
length. 


2 U. S. Geol. Survey, Geol. Atlas, Atoka Folio, No. 79, 1902. 

3 IJ. S. Geol. Survey, Geol. Atlas, Tishomingo Folio, No. 98, 1903. 

4 Okla. Geol. Survey, Bull. No. 3, p 32, 1910. 

5 Amer. Assoc. Pet. Geologists, vol. 6, p. 421, 1922. 







ARBUCKLE LIMESTONE 


23 


Taff 6 also noted conglomerates in the basal part of the Ar>- 
buckle limestone. The lower conglomerates were not observed by 
the writer. It is possible that all the clastic beds represent re¬ 
worked portions of the Arbuckle itself. The fragments which con¬ 
stitute the higher conglomerates, however, indicate a source outside 
of the immediate area. The variation in sedimentation shown by 
the occasional conglomerates suggests warping movements within 
the area during the time at which the formation was being deposited. 

FOSSILS 

The following fossils from the Arbuckle limestone were identi¬ 
fied by Ulrich and Walcott and were published by Taff 7 . 

Fossils of upper portion of Arbuckle limestone. 

(Identification by E. O. Ulrich) 

Billingsella, 2 species 
Polytoechia ? 

Stromatocerium 

Calathium, 2 species 

Maclurea 

Ophileta 

Eccyliomphalus 

Eccyliopterus 

Raphistomina 

Leiospira (? Helicotoma)) 

Euconia (near E. ramsayi Billings) 

Hormotoma, 2 species, one very near H. artemesia Billings. 

Trochonema 

Orthoceras 

Trochoceras 

Leperd.itia 

Isochilina 

Primitia 

Bathyurus 

Isotelus canalis? 

Fossils of lower portion of Arbuckle limestone 

(Identification by Walcott) 

Dikelocephalus sp. undetermined 
Dikelocephalus (?) cf. augustifrous 
Illaenurus cf. eurekensis Walcott 
Illaenurus sp. undetermined 
Syntrophia sp. undetermined 

AGE AND CORRELATION 

The fossils identified by Walcott are from the lower 700 feet 
of the formation and are all upper Cambrian types. 

The fossils of Ulrich’s identification are from zones ranging 
from 2,000 feet above the highest known upper Cambrian forms to 


6 Taff, J. A., U. S. Geol. Survey, Prof. Paper No. 31, p. 22, 1904 

7 Idem. 



24 


ARBUCKLE LIMESTONE 


the top of the formation. They indicate lower Ordovician age for 
the upper portion of the Arbuckle limestone. 

Dake 8 has suggested a correlation of the upper Arbuckle lime¬ 
stone with the Powell, Cotter, Jefferson City, Roubidoux, Gascon¬ 
ade, and Gunter of Arkansas, Missouri and Illinois; and the Shako- 
pee, New Richmond, and Oneota of Iowa and Wisconsin. He cor¬ 
related the lower Arbuckle with the Potsdam. (See Plate II) 

STRUCTURE 

Faulting along the borders of the Arbuckle outcrop as it is ex¬ 
posed in the Stonewall quadrangle is the rule rather than the excep- 

PLATE V 



A CROSS-BEDDED, CONGLOMERATIC SANDSTONE IN THE UPPER PART 
OF THE ARBUCKLE LIMESTONE IN SEC. 29, T. 1 N„ R. 7 E 

tion. At one place, in the northeast corner of T. 1 N., R. 6 E., the 
formation is in contact with Viola limestone which normally occurs 
in the section about 1,500 feet above the top of the Arbuckle. 

For most of the distance around the edge of the outcrop the 
formation is succeeded by strata of Ordovician age, but at two 
points, along the western side, Arbuckle strata pass beneath over¬ 
lapping conglomeratic beds of late Pennsylvanian age. 


8 Dake, C. L. The Problem of the St. Peter Sandstone, School of Mines and 
Metallurgy, University of Missouri, Bull., vol. 6, No. 1, 1921. 




SIMPSON FORMATION 


25 


ECONOMIC IMPORTANCE 

The chief economic use of Arbuckle limestone is for road 
metal, railroad ballast, and concrete rock. 

SIMPSON FORMATION 

NAME 

The original description of the Simpson formation is by Taff 9 
Although not definitely so stated by that author, it is probable that 
the name was derived from the village of Simpson, situated in the 
northeastern part of T. 1 S., R. 6 E. No section of the formation 
for the area around Simpson was given. 

AREAL DISTRIBUTION 

The outcrop of the formation in the Stonewall quadrangle 
appears as a faulted and discontinuous band bordering the Ar¬ 
buckle outcrop. There is also a small outlier of the formation near 
the center of T. 1 N., R. 5 E. Because of its lack of continuity the 
outcrop of the formation may conveniently be divided into an east¬ 
ern, a western, a northern, and a central portion. 

The eastern exposure represents the northern portion of what 
Buttram 10 has called the Delaware Creek area. The dip of the 
formation here is normally eastward and ranges from three to as 
much as 20 degrees. Extending in a northeast-southwesterly direc¬ 
tion through secs. 19, 20, 21, and 30, T. 1 N., R. 7 E., a fault cuts 
the formation. In common with all the faulting in this area the 
upthrow side of the displacement occurs on the south side. This 
condition coupled with subsequent planation has resulted in an east¬ 
ward offset of the portion of the outcrop which occurs to the south 
of the fault. I ' 

The western exposure, termed by Buttram 11 the Hickory area, 
is located near the center of T. 1 N., R. 4 E. Faults border this 
area along the northern, southern, and eastern sides and bring beds 
above the base of the formation into contact with the Arbuckle 
limestone. Along its western side the exposure passes beneath 
overlapping beds (Vanoss) of very late Pennsylvanian age. 

Probably as a result of the movement along the bordering 
faults, the general structural expression of the area is basin-like. 
There are folded portions within the basin, however, as is shown 
by the northward dip of the strata in the glass sand pit just north of 
Hickory. (Plate VI.) 

To be considered with this western area, but not visibly con- 


9 Taff, J. A., U. S. Geol. Survey, Geol. Atlas Atoka Folio No. 79, 1902. 

10 Buttram, Frank, Okla. Geol. Survey, Bull. 10, p. 58, 1913. 

it Idem. p. 69. 



26 


SIMPSON FORMATION 


nected with it, is a small exposure of Simpson in the southwest 
corner of T. 1 N., R. 4 E., and the northwest corner of T. 1 S’., R, 
4 E. This represents a northern projection into the Stonewall area 
of a large outcrop of the formation which occurs in the Tishomingo 
quadrangle. 

The northern or Roff area is roughly hook-like in form with 
the concave side southward. The point of the hook lies about two 
miles south of Roff while the narrow shank-like portion may be 
traced 1 , southward to the north central part of T. 1 N., R. 6 E. 
There are faults along the north and south border of the exposure. 
To the west, however, the formation is overlapped by Pennsylvanian 
(Ada) beds. 

The central area consists of a small synclinal outlier which is 
located near the central part of T. 1 N., R. 5 E. 

The exposure of the formation in the four areas as here de¬ 
scribed totals approximately 25 square miles. 

THICKNESS AND CHARACTER 

The thickness of the Simpson has been given 12 as ranging from 
1,200 to 2,000 feet. 

The variation in thickness is explained by Taff as being the re¬ 
sult of the local absence of the basal portion of the formation, so 
that here again there is evidence of a probable early warping move¬ 
ment of the Arbuckle mountain area. 

Near the center of the formation is a thick sandstone 
member (100 to 200 feet) which is more persistent than the 
others. 

Regarding the general character of the formation Taff 13 says: 

In the northern portion of the region, and especially on the northern 
side of the Arbuckle Mountains west of Washita River, the Simpson for¬ 
mation is found to be much thinner than in the southern portion. This is 
due chiefly to the absence of the lowest beds, which have an aggregate 
thickness of several hundred feet. The upper division of the formation 
is found to become thinner northward, owing to the decrease in the 
quantity of lime and clay. With the decrease in the amounts of lime and 
clay northward there is a general increase in the abundance of sand, the 
whole formation becoming more siliceous. 

The absence of the lower portion of the formation toward the 
north and the more clastic nature of subsequent portions of the 
formation in that direction, suggest an Ordovician land mass to the 


a2 Taff, J. ,A., U. S. Geol. Survey, Geol. Atlas Tishimingo Folio No. 98, 1903. 
13 U. S. Geol. Survey, Prof. Paper, No. 31, p. 24, 1904. 



SIMPSON FORMATION 


27 


north of the Arbuckle area over which the Simpson sea gradually 
encroached. The possibility of a land mass in that same general 
region is again suggested by a similar northward variation in the 
formations comprising the Hunton terrane. 

In the Doan well, drilled in the northeast corner of sec. 20, T. 5 
N., R. 4 E., the Simpson formation was encountered at a depth of 
2,955 feet and was penetrated for 355 feet. For a section of the 
portion here penetrated, see the log of this well given under head¬ 
ing ‘‘Well Logs.” 

The formation has also been encountered in three other wells 
drilled in the Stonewall quadrangle at the localities and depths 
listed : 

SE. cor., sec. 11, T. 2 N., R. 3 E., 810 
SE. cor., sec. 34, T. 4 N., R. 4 E., 1,960 
NW. cor., sec. 16, T. 4 N., R. 4 E., 1,985 

For logs of these wells see discussion of well logs. 

The less resistant nature of the Simpson formation, as compar¬ 
ed with the underlying Arbuckle limestone and the overlying Viola 
limestone, generally results in its more rapid erosion. For this 
reason stream valleys often occupy the areas in which the formation 
is exposed. 

FOSSILS 

Taff 14 lists the following fossils from the Simpson formation: 

' Fossils of upper Simpson formation 

Receptaculitles sp. nov. 

Protarea sp. nov. (Massive-laminar form) 

Archaeocrinus sp. undetermined 
Platycystites (?) sp. nov. 

Amygdalocystites sp. nov. 

Glyptocystites sp. nov. 

*Numerous monticuliporoid Bryozoa 
Stomatopora proutana-pertenuis Ulrich 
Phylloporina sublaxa Ulrich 
Rhinidictya nicholsoni Ulrich 
Arthroclema sp. nov. 

Pachydictya cf. foliata Ulrich 
Lingula coburgensis Billings 

Schizambon (? Siphonotreta) minnesotensis H. and C. 
Crania granulosa Winchell 
Craniella ? ulrichi Hall 
Pholidops trentonensis Hall 


14 Taff, J. A., U. S. Geol. Survey, Prof. Paper No. 31, pp. 24 and 25, 1904. 



28 


SIMPSON FORMATION 


Fossils of upper Simpson formation 

Plectambonites sericea (Stones River variety) 

Strophomena filitexta Hall 
Rafinesquina minnesotensis Winchell 
Scenidium anthonense Sardeson 
*Orthis tricenaria Conrad 
*Dalmanella perveta Conrad 
*Dinorthis near pectinella Emmons 
*Orthis (? Dinorthis) deflecta Conrad 
Orthis (? Dinorthis) sp. nov. 

Hebertella bellarugosa Conrad 
Triplecia sp. nov. (striated) 

Zygospira (Hallina) nicolleti W. and S. 

Zygospira (Hallina) sp. nov. 

Clionychia lamellosa Hall 

Ctenodonta contracta Salter 

Eurymya plana Hall 

Tetranota obsoleta ? Ulrich 

Pterotheca attenuata Hall 

Ampyx sp. undetermined 

Harpina sp. undetermined 

Platymetopus sp. nov. near bicornis Ulrich 

Platymetopus sp. nov. near cucullus M. and W. 

Pterygometopus near schmidti Clarke 

Numerous undetermined small Ostracoda of the families 
Cypridae and Beyrichiidae 

Fossils of lower Simpson formation. 

Plates of cystidian (? Glyptocystites) 

Siphonotreta sp. undetermined 
Crania sp. nov. 

Orthis costata 

Orthis (Dalmanella) pogonipensis Walcott 
Orthis sp. ? nov. (near holstoni Safford) 

Ctenodonta sp. nov. (of C. nasuta type) 

Ctenodonta sp. nov. (large, ovate species) 

Cyrtodonta sp. undetermined 
Modiolopsis sp. nov. 

Modiolopsis sp. nov. 

Bucania sp. undet. (small, with flat dorsum) 

Bucania sp. undet. (larger, with subcarinate dorsum) 
Bucanella sp. undetermined 


*Most of these species known only in the upper 300 feet. Those occurring 
also in the lower part of the subdivision are distinguished by an asterisk. 



PLATE VI 



NORTHWARD DIPPING SIMPSON STRATA IN 
GLASS SAND PIT NORTH OF THE TOWN 
OF HICKORY 





30 


VIOLA LIMESTONE 


Fossils of lower Simpson formation 

MacJurea sp. undetermined 
Eccyliopterus sp. undetermined 
Leperditia sp. near fabulites 
Leperditia sp. near fabulites 
Leperditia bivia White 

Leperditella of several undetermined species 

This division is particularly characterized by these 
Ostracoda, many of the limestone layers being crowded 
with large and small species. 

Bathyurus sp. undetermined 
Ceraurus of two undetermined species 
Amphion nevadensis ? Walcott. 

AGE AND CORRELATION 

The conclusions drawn from these fossil lists were that: 

The fauna of the lower division of the Simpson formation is decided! 1 .' 
similar to that of the Chazy of New York and Canada and of the Pogonip 
formation of Nevada. Considering these east and west connections, it is 
surprising to note that the lower Simpson fauna, so far as known, contains 
none of the prolific fauna of the lower division (Murfressboro limestone) of 
the Stones River group in Middle Tennessee, which is believed to be of 
equivalent age. As a whole the fauna of the upper part of the Simpson 
is closely related to the upper division of the Stones River group in Ten¬ 
nessee and Kentucky and the equivalent beds in the upper pa t of the Mis¬ 
sissippi Valley. (See Plate II for a correlation suggested by Dake.) 

STRUCTURE 

The structure of the Simpson formation is in general like that 
of the Hunton limestone and is shown in Plate VII. 

ECONOMIC IMPORTANCE 

The Simpson is important economically for the sand asphalt 
and glass sand deposits which it contains. These resources are 
discussed in publications of the Oklahoma Geological Survey . 15 

VIOLA LIMESTONE 

NAME 

This formation was named by Taff 16 after the village of Viola, 
which is located close to the outcrop of the formation five miles 
west of Wapanucka. 

15 Snider, L. C., Rock Asphalts of Oklahoma and their use in paving. 

Okla. Geol. Survey, Circular No. 5, 1913. 

Buttram, Frank, Glass Sands of Oklahoma, Okla. Geol. Survey, Bull. No. 

10, 1913. 

16 Taff, J. A., U. S. Geol. Survey, Geol. Atlas, Atoka Folio, No. 79, p. 3, 1902. 



VIOLA LIMESTONE 


31 


AREAL DISTRIBUTION 

The Viola limestone is exposed at four places in the Stonewall 
quadrangle: 

1. In the southeast corner of the area where it outcrops over 
an area of about 15 square miles. 

2. As a narrow band along the south side of the Franks 
graben, with an extent of approximately three miles. 

3. On the Lawrence uplift where the areal exposure extends 
over about 15 square miles, and 

4. As a small inlier northwest of Lawrence, in secs. 26, 2 7, 
34, and 35, T. 3 N., R. 5 E. 

THICKNESS AND CHARACTER 

The thickness of the Viola is between 500 and 750 feet. The 
following section was measured across portions of secs. 12 and 
13, T. 1 N., R. 6 E. 

Section of the Viola limestone as exposed in secs. 12 and 13 , T. 1 


N., R. 6 B. 

Feet 

Blue and white limestone with some chert_100 

Gray and blue limestone with little or no chert-90 

Massive limestone bed_ 10 

White argillaceous limestone_ 3 

Massive blue limestone bed- 10 

Medium to thin-bedded limestone_3 5 

Limestone with sand lentils___15 

Limestone with interbedded shale lentils. The lime¬ 


stone in this portion Is white or whitish gray on 
fresh exposures, but weathers to a dark gray and 
through differential weathering develops a rough 


pitted surface-3 5 

Possiliferous limestone with some chert_25 

Thin-bedded limestone with chert_95 

Thin-bedded limestone without chert-30 

Massive blue limestone- 4 

Granular white limestone-120 

This portion of the formation is platy near 
its upper limit and there weathers more rapidly 
so that streams and gullys often mark the zone. 

Shale with thin beds of limestone-45 

Very fossiliferous limestone bed- 2 

Argillaceous limestone - 5 

Thin-bedded limestone and shale-10 

Dense white limestone (Base of formation)- 3 


637 




















32 


VIOLA LIMESTONE 


No other sections of the Viola limestone were measured, but 
the evidence afforded by wells drilled in the western and northern 
portions of the quadrangle indicates that the formation thins in that 
direction. In the well at Vanoss (sec. 34, T. 4 N., R. 4 E.) there is 
apparently 660 feet of limestone assignable to the Viola, while in 
the Doan Well (sec. 20, T. 5 N., R. 5 E.) there seems to be only 
190 feet of the formation. 

In color the strata of the Viola range through whitles and 
grays. 

An interesting contribution to the general description of the 
Viola limestone is by Howell 17 in which it is pointed out that there is 
little or no dolomite in the formation. The importance of this ob¬ 
servation lies in the fact that while there is quite often a close 
lithologic similarity between the Viola and the much older Arbuckle 
limestone, the latter normally carries about 10 percent of dolomite. 
By taking advantage of this difference a method is afforded for dis¬ 
tinguishing between well cuttings from the two formations. 

FOSSILS 

Ulrich identified the following fossils from the Viola limestone 
and the lists were subsequently published by Taff. 18 

Fossils of the upper portion of Viola limestone 

Bead-like joints of the stalk of an undescribed crinoid or 
cystid, one-quarter inch in thickness. 

Pachydictya gigantea Ulrich 
Ptilotrypa obliquata Ulrich 

Plectambonites sp. nov. (with denticulate hinge) 
Strophomena wisconsinensis Whitfield 
Leptaena unicostata M. and W. 

Rafinesquina sp. nov. (near camerata) 

Orthis kankakensis sweeneyi Winchell 
Dinorthis subquadrata Hall 
Dinorthis proavita W. and S. 

Hebertella insculpta Hall 
Dalmanella macrior Sardeson 
Platystrophia acutilirata Conrad 
Rhynchotrema capax Conrad 
Parastrophia divergens H. and C. 

Fossils of the middle portion of Viola limestone 
Diplograptus pristis? Hall 
Climacograptus typicalis Hall 

17 Howell, J. V., Am. Assoc. Pet. Geologists, vol. 6, p. 413, 1922. 

18 Taff, J. A., U. S. Geol. Survey, Prof. Paper No. 31, pp. 26-27, 1904. 



VIOLA LIMESTONE 


33 


Fossils of the middle portion of Viola limetone. ( Continued ) 

Schizotreta minutula W. and S. 

Conotreta, sp. undetermined (? rusti Walcott) 

Rafinesquina deltoidea Conrad. 

Conularia trentonensis Hall 
Trinucleus concentricus Eaton 
Trinucleus sp. undetermined 
Proetus parviusculus var. 

Pterygometopus (near callicephalus Hall) 

Nileus vigilans Meek and Worthen 

Fossils of lower portions of Viola limestone 

Streptelasma profundum var. 

Tetradium columnare Hall 
Homotrypa intercalaris Ulrich 
Bythopora subgracilis Ulrich 
Phylloporina reticulata Hall 
Rhinidictya mutabilis Ulrich 
Rhinidictya mutabilis major Ulrich 
Escharopora subrecta Ulrich 
Phaenopora incipiens Ulrich 
Arthropora bifurcata Ulrich 
Plectambonites sericea var. 

Strophomena filitexta Hall. 

Rafinesquina deltoidea Conrad 
Dalmanella hamburgensis ? Walcott 
Dinorthis pectinella Hall 
Platystrophia sp. undetermined (small) 

Rhynchotrema increbescens Hall 
Zygospira recurvirostris Hall 
Vanuxemia gibbosa Ulrich 
Technophorus subacutus? Ulrich 
Cyrtolites retrorsus Ulrich 
Protowarthia pervoluta U. and S. 

Lophospira bicincta Hall 
Strophostylus textilis U. and S. 

Holopea obliqua ? Hall. 

Pterotheca attenuata Hall 
Bumastus trentonensis Emmons 

Ulrich has shown that the Viola contains three faunal zones. 
From his study of the fossils it was concluded that there is a varia¬ 
tion in the thickness of the lower portion of the formation which is 
apparently due to the local absence of beds. 

The absence of beds again suggests the probability of early 
warping movements in the Arbuckle area. 

AGE AND CORRELATION 

From the faunal evidence Ulrich concluded that the lower por- 


34 


SYLVAN SHALE 


tion of the Viola is probably equivalent to the latest Black River and 
earliest Trenton of New York and Canada; that the middle por¬ 
tion is of late Trenton age; and that the fossils of the upper portion 
of the formation are species characterizing the upper divisions of 
Richmond age in Minnesota, Illinois, Indiana, and Ohio, while they 
are also characteristic of the Polk Bayou limestone of Northern 
Arkansas and the Fernvale formation of Middle Tennessee. For a 
correlation suggested by Dake see Plate II. 

STRUCTURE 

In the southeastern part of the Stonewall quadrangle the Viola 
limestone dips toward the east and northeast and is cut by several 
faults. Neither folding nor faulting are so intense here, however, 
as in the area west and north of Franks. On the Lawrence uplift, 
especially along its flanks, faults are also present. On the central 
part of the uplift, however, the formation is inclined at low angles. 
For this reason the outcrop in this locality extends over a compara¬ 
tively large area. 

The inlier mentioned as occurring in secs. 26 , 27, 34, and 35, 
T. 3 N., R. 5 E., is not shown on earlier maps. It is of importance 
in clearly indicating the overlapping nature of the upper Pennsylvan¬ 
ian strata on the flanks of the Arbuckle Mountains. Along the 
creek in the northwestern part of section 27 the Viola limestone 
dips from 5 to 8 degrees northeastward while the Pennsylvanian 
strata (at this point Seminole formation) which immediately overbe 
it are inclined at about 10 degrees toward the west 

ECONOMIC IMPORTANCE 

The Viola limestone is used as road metal and in the manu¬ 
facture of Portland cement. A large quarry at Lawrence furnishes 
Viola limestone to the Oklahoma Cement Plant at Ada. An asphalt 
impregnated phase of the formation is quarried for paving purposes 
at a point a few miles southwest of Sulphur. 

SYLVAN SHALE 

NAME 

The Sylvan shale was first described by Taff. 19 It takes its 
name from the village of Sylvan, in the central part of the Tishi- 
mingo quadrangle, near which it is typically exposed. 

AREAL DISTRIBUTION 

The formation is exposed as a discontinuous, ribbon-like out¬ 
crop from the southeastern part of the Stonewall quadrangle north¬ 
westward to the western end of the Franks graben. Here it turns 
sharply northeastward to the crest of the Lawrence uplift after 


19 U. S. Geol. Survey Geol. Atlas, Atoka Folio, No. 79, p. 3, 1902. 



SYLVAN SHALE 


35 


which it again follows a general northwesterly course to a point just 
north of Lawrence. At the latter place it is overlapped by Pennsyl¬ 
vanian strata. 

Local absence of the formation at points along the trend of 
the outcrop has resulted from faulting, sharp folding with attendant 
squeezing of this incompetent formation, and overlap. All three 
factors have modified the Sylvan outcrop along the flanks of the 
Franks graben. 

The linear extent of the Sylvan outcrop, within the Stonewall 
quadrangle, is about the same as that of the other older Paleozoic 
formations. Because of the facts, however, that it is only exposed 
in the more highly folded regions and that it is much thinner than 
most of the other formations, its areal extent is comparatively small. 

THICKNESS AND CHARACTER 

The thickness of the Sylvan, according to Taff 20 , increases 
from 60 feet at the east end of the Arbuckle uplift to approximately 
300 feet west of Washita River. 

In the quarry, just east of Lawrence a full section of the Sylvan 
is exposed and here totals approximately 120 feet. Complete sec¬ 
tions are also available from the logs of two wells drilled in the 
Stonewall quadrangle. In the first of these located in the center of 
sec. 12, T. 3 N., R. 7 E., the Sylvan has a thickness of 151 feet and 
in the other, situated in the northeast quarter of sec. 20, T. 5 N., R. 
4 E., it is 145 feet thick. 

These sections indicate a thickening of the formation northward 
as well as westward. 

On fresh exposures the Sylvan shale is generally green or 
greenish-blue in color. Because of the lack of resistant beds within 
the formation it weathers rapidly, resulting quite commonly in un¬ 
dercutting of the succeeding Chimneyhill limestone, so that an 
abrupt escarpment often marks the contacts of the two formations. 
This is the case east of Lawrence. 

FOSSILS 

Fossils have never been found in the Sylvan except in its basal 
portion at one point about two miles north of Dougherty. Taff 21 
lists the following species which were collected from that point. 

Diplograptus sp. undet., Climacograptus sp. near 
typicalis, Leptograptus sp. undet., Lingula; short, obtuse 
form. Lingulops? sp. nov. (platform obsolete), Leptobo- 


20 U. S. Geol Survey, Prof. Paper No. 31, p. 28, 1904. 

21 U. S. Geol. Survey, Prof. Paper, No. 31, p. 28, 1904. 



36 


HUNTON TERRANE 


lus sp. near insignis, Leptobolus? sp. nov. (has six strong 
radiating plications), Conularia sp. nov., with surface 
sculpture very similar to that of the Trenton C. papillata 
Hall. Conodonts of forms resembling those referred by 
Hinde to Prioniodus and Polygnathus 

AGE AND CORRELATION 

From the evidence afforded by this faunule Taff 22 concluded 
that the Sylvan shale should be correlated with the Medina and 
that the line separating the Ordovician and Silurian in the Arbuckle 
Mountains should be placed between the Viola limestone and the 
Sylvan shale. 

Professor Schuchert 23 correlates the Sylvan with the Maquo- 
keta shale of Missouri, Iowa, and Minnesota. 

ECONOMIC IMPORTANCE 

The Sylvan shale is quarried at Lawrence and used in great 
quantities for the manufacture of Portland cement. 

HUNTON TERRANE 

NAME 

To the series of limestones, marls and shales which succeed the 
Sylvan shale, Taff 24 gave the name Hunton formation. The name 
is after the town of Hunton in the Atoka quadrangle near which the 
type section is exposed. 

In a later publication by Reeds 25 the strata are divided into 
four separate formations. Since the formations belong to two ge¬ 
ologic systems the term Hunton is no longer used as a formational 
name. It is here retained as the name of a terrane in which is 
included the group of formations which constitute the original unit 
as defined by Taff. In the present investigation sufficient time was 
not available to map the several formations proposed by Reeds and 
the limits of the Hunton terrane as shown on the accompanying map 
are therefore in accord with those given by Taff for the Hunton 
formation. 


AREAL DISTRIBUTION 

In the southeastern part of the Stonewall quadrangle the Hun¬ 
ton outcrop is narrow and discontinuous; the local points of non-ex- 

22 Idem. p. 29 

23 Statement by Reeds, Okla. Geol. Survey, Bull. No. 3, p. 39, 1910. 

24 TafF, J. A., U. S., Geol. Survey, Geol. Atlas, Atoka Folio, No. 79, p. 3, 1902. 
25 Reeds, Chester A., The Hunton Formation of Oklahoma, Amer. Jour. Sci. 
vol. XXXII, October 1911. 



CHIMNEYHILL LIMESTONE 


37 


posure being due to faulting and overlap. In the northern part of 
T. 2 N., R. 6 E., and in the southwestern part of T. 3 N., R. 6 E., 
however, it is exposed over an area of some nine square miles on the 
crest and northern flank of the Lawrence uplift. Farther north 
Hunton beds have been encountered in several deep wells. 26 

The locations of these wells and the depths at which such strata 


were encountered are as follows: 

Northeast quarter sec. 28, T. 3 N. R. 7 E_1,160 

Center sec. 12, T. 3 N., R. 7 E_2,310 

North center sec. 4, T. 4 N., R. 5 E_2,302 

Northeast cor. sec. 14, T. 5 N., R. 4 E_ 2,675 

Northeast cor. sec. 20, T. 5 N., R. 4 E_2,500 

Northwest cor. sec. 16, T. 4 N., R. 4 E_1,595 


Evidence of the presence of Hunton formations in the first 
two wells listed rests on lithologic character, stratigraphic succes¬ 
sion, and agreement of probable depth with structural conditions. 
In addition to this evidence, the presence of Hunton in the last 
four wells is established by a collection of fossils taken from cut¬ 
tings secured from the well in sec. 4, T. 4 N., R. 5 E. Confirma¬ 
tion of the age of the fossils was given by Profjessof Galloway of 
Columbia University. 

Hunton fossils were also secured from the oil producing sand 
in the deep well southeast of the town of Maud and confirmed as 
such by Professor Schuchert of Yale University. 

THICKNESS AND CHARACTER 

Reeds’ divisions of the Hunton with their thickness and cor¬ 
relation may best be shown by here including one of his tables. 

DIVISIONS 

CHmNEYHILL LIMESTONE 

DESCRIPTION 

This formation takes its name from Chimneyhill Creek (South 
Fork of Jack Fork Creek on most maps). The type section is at 
the confluence of three small creeks in sec. 4, T. 2 N., R. 6 E. The 
formation is easily recognized by its Pink-Crinoidal and Oolitic mem¬ 
bers. The Chimneyhill limestone is especially well exposed in the 
region east of Lawrence where it caps a westward-facing escarp¬ 
ment of Sylvan shale. The contact is one of unconformity. Good 
exposures of the limestone are also common farther southeast where 


*’ 6 For a more detailed discussion of these occurrences see Circular No. 10, 
Paper No. 1, of the Oklahoma Geological Survey. 








38 


CORRELATION TABLE 


Correlation table of the Siluro-Devonian rocks, Arbncklc Mountains. 

Oklahoma. 


Oh 


m 


be 

d 


Reeds 1911 


Taff, Ulrich, and 
Girty 
1903-1904 


jpj 

33 


pi 

’So 




<3 


o 

a> 


'zi 

* d 

£ ? 

v 

m 




<D 

cS 

(h 

dS 

Pi 

•rH 

d 

d 

> 

be 

etj 

rO 

o 

'qj 

X! 

2 

pq 

o 

hP 


.5 

5 


^3 

o 


Bois d’Arc limestone 
0-90 feet, average 60 feet 


Upper 

Hunton 


Haragan shale 

0-166 feet, averages 100 feet 


-BREAK- 


Henryhouse shale 
0-223 feet, average 90 feet 


-BREAK- 


Middle 

Hunton 


Chimney hill j 
limestone 
0-53 feet 
Av. 35 ft. 


Pink-Crinoid member 
0-39 ft., average 
15 ft. 

Glauconitic member 
0-25 ft., Av. 15 ft. 

Oolitic member 
0-12 ft., Av. 5 ft. 


Lower 

Hunton 


pi 

c6 


Pi 

ei 

•rH 

boo 


w 


Pi 

d 

ce 

be 

d 


Pi 

o 

-M 

• |H 

6 




























HENRYHOUSE SHALE 


39 


the several formations of the Hunton terrane extend along the 
northeastern flank of the main mass of the Arbuckle Mountains. 

fossils 

Reeds lists the following fossils as most characteristic of the 
Chimneyhill formation. 

Oolitic Member 

Atrypa n. sp., Schuchertella sp., Rhipidomella n. sp., Cyclo- 
nema daytonensis. 


Glauconitic Member 

Callopora magnopora, Pachydictya bifurcata, Phenopora fim- 
briata, Phenopora magna, Rhinopora verrucosa, Plectambonites 
transversalis n. var., Strophomena (?) antiquata, Cyclonema ven- 
tricosa, Orthoceras cf. latanummulatum, Illaenus ambiguas, Illaenus 
cf. armatus. 


Pink-Crinoidal Member 

Pisocrinus sp., Homoeospira n. sp., Plectambonites tenn- 
esseensis (Cf. quinquecostata McCoy), Spirifer radiatus, Stropheo- 
donta corrugata, Triplecia n. sp., (cf. waldronensis), Whitfieldella 
sp., Delthyris, n. sp., Conocardium sp., Hyolithes n. sp., Lophospira 
sp., Calymene sp. Cyphaspis clintonensis, Dalmanites arkansus, 
Illaenus 2 sp., Lichas n. sp., Odontopleura arkansana; Proetus 
corrugatus? Proetus determinatus? Sphaerexochus sp. 

HENRYHOUSE SHALE 

DESCRIPTION 

The formation derives its name from Henryhouse Creek which 
crosses the outcrop at a point about three miles east of Woodford 
in Carter County. 

According to Reeds the Henryhouse shale rests unconformably 
upon the Chimneyhill limestone. It is thickest in the western part 
of the Arbuckle Mountains and thins eastward so that in the Stone¬ 
wall quadrangle it is entirely absent between Canyon Creek and the 
southeast corner of the quadrangle. Thinning toward the north is 
apparently less rapid because the fossils secured from the well in 
sec. 4, T. 4 N., R. 5 E., indicate its presence at that point. 

As is indicated by its name the Henryhouse shale consists large¬ 
ly of shales. Within these, soft marly limestones are interbedded, 
and there are occasional resistant limestone beds which, due to dif¬ 
ferential weathering, stand out as small ridges. 

FOSSILS 

The following species have been listed by Reeds as character¬ 
istic of the formaton. 


40 


HARAGAN SHALE 


Lozwer Henryhouse 

Glassia sp., Scenidium insigue, Schuchertella n. sp., Stropheo- 
donta n. sp., Strophonella prolongata, Platyschisma n. sp., Ortho- 
ceras n. sp., Bronteus cf. plana, Ceraurus niagarensis, Palmanites 
n. sp., Encrinurus n. sp., 

Upper Henryhouse 

Astylospongia praemorsa, Amplexus shumardi, Aulopera re¬ 
pens, Calceola sp., Cladopora reticulata, Eridophyllum rugosum, 
Favosites venustus n. var., Heliophyllum radiculum, Plasmopora 
follis, Thecia minor, Thecia major, Coccoseris micropora, Heliolites 
interstinctus, Heliolites subtuberlatus, Pisiocrinus milliganae, Syn- 
bathocrinus tennesseenis, Ascodictyon silurinense, Bythotrypa cf. 
distichia, Bythotrypa cf. squamata, Chilotrypa 4 sp., Crepipora n. 
sp., Fenestella cf. acuticosta, Fistulipora 2 sp., Hederella sp., Lepto- 
trypa n. sp., Lioclema 2 sp., Nicholsonella cf. florida, Penniretepora 
cf. distichia, Rhopalonaria attenuata, Anastrophia cf. internascens, 
Anoplotheca saffordi, Atrypa cf. nodostriata. Camarothoechia? 
neglecta, Herbertella fissiplica, Leptaena sp. (European type), 
Nucleospira cf. lentiformis, Pholidops sp., Rhynchonella n. sp., 
Rhynchospira globosa, Schuchertella subplanus, Spirifer crispus, 
Strophonella tenuistriata, Uncinulus cf. nucleolata, Uncinulus cf. 
stricklandi, Amphicoelia sp., Platystoma sp., Cyrtoceras subrectum, 
Orthoceras sp., Acaste cf. dowingae, Dalmanites n. sp. 

HARAGAN SHALE 

DESCRIPTION 

The term Haragan was given by Reeds to an unnamed creek 
in the Ardmore quadrangle in sec. 17, T. 2 S., R. 3 E., and from 
this he derived the name of the formation. Three to four miles 
southeast of Dougherty there are excellent exposures of the forma¬ 
tion along the creek mentioned and this region was taken as the 
type area. 

In the Stonewall quadrangle the Haragan shale is apparently 
absent on the Lawrence uplift, but is very well exposed in the out¬ 
crop of the Hunton formations in the southeastern part of the quad¬ 
rangle. 

Lithologically the Haragan greatly resembles the underlying 
Henryhouse shale and in the absence of fossils it is very doubtful 
whether the two could be distinguished. 

FOSSILS 

Species determined by Reeds to be peculiar to the Haragan 
are the following: 


BOIS D’ARC LIMESTONE 


41 


Favosites venustus, Striatopora issa, Brachiocrinus sp., 
Edriocrinus n. sp., Callopora perelegans, Anoplia helderbergae, 
Atrypa nodostriata n. var., Atrypina imbricata, Camarotoechia 
bialveata, Chonetes sp., Cyrtina dalmani, Dalmanella n. sp., Dal- 
manella subcarinata, Arthostrophia strophomenoides, Spirifer cyc- 
lopterus n. var. Stropheodonta crebristriata, Stropheodonta varis- 
triata, Stropheodonta n. sp., Stropheodonta cf. planulata, Strophon- 
ella n. sp., Trematospira cf. costata, Conocardium sp., Megambonia 
sp., Diaphorastoma n. sp., Diaphorostoma ventricosa, Platyceras 
lamellosum, Platyceras unguiforme, Pleurotomaria n. sp., Tenta- 
culites gyracanthus, Dawsonoceras n. sp., Dicranurus hamatus, 
Phacops logani. 

From his faunal studies Reeds concluded the age of the Hara- 
gan to be New Scotland and since the underlying Henryhouse is 
Niagaran the unconformable contact between the two is also the 
line between the Silurian and the Devonian. 

BOIS D’ARC LIMESTONE 

DESCRIPTION 

The Bois d’Arc limestone takes its name from, and its type 
area is located along, the creek of that name in sec. 4, T. 2 N., 
R. 6 E. It contains near its top several thin beds of chert, from 
which numerous float pebbles are generally scattered along the 
outcrop. Chert is probably the most characteristic lithologic fea¬ 
ture of the formation, but the formation may sometimes be recog¬ 
nized also by the granular, crystalline limestone beds which it con¬ 
tains. The limestone beds are white on fresh exposures, but 
weather to a dirty-gray color. 

The Bois d’Arc is locally absent and in such places the suc¬ 
ceeding Woodford formation rests directly upon the older forma¬ 
tions of the Hunton terrane. Reeds 27 mentions such a place in the 
vicinity of Honey creek near Washita River. Other localities in 
which such absence has been observed are sec. 22, T. 1 N., R. 7 E., 
at which point the Woodford apparently rests directly upon the 
Haragan shale, and along the northern flank of the Lawrence up¬ 
lift in secs. 29 and 30, T. 3 N., R. 6 E. A well drilled in the center 
of sec. 16, T. 3 N., R. 6 E., indicates that there is only 80 feet of 
Hunton there. It appears, therefore, that in addition to absence of 
the Haragan shales from the Lawrence uplift, most of the Henry- 
house is also absent. The well log indicates 40 feet of Chimney- 
hill and 40 feet of Henryhouse with the Woodford chert resting 
on the latter. 


27 Reeds, Chester A., Amer. Jour. Sci., vol. XXXII, p. 264, Oct. 1911. 



42 


WOODFORD FORMATION 


FOSSILS 

The following are given by Reeds as characteristic species of 
the Bois d’Arc limestone: 

Dendropora n. sp., Favosites shriveri, Trachypora n. sp., 
Pisocrinus sp., Codaster n. sp., Cyrtina rostrata, Eatonia, singularis, 
Leptostrophia magnifica, Leptostrophia oriskania, Meristella laevis, 
Meristella lentiformis, Rensselaeria marylandica, Spirifer concinnus, 
Spirifer cyclopterus, cf. hartlei, Stropheodonta becki, Strophonella 
cavumbona, Trematospira n. sp., Uncinulus 2 n. sp., Mytilarca cf. 
acutirostra, Orthonychia cf. plicatum, Platyceras n. sp., cf. teniul- 
iratum. 


STRUCTURE 

The complex structure of the Hunton strata is shown on the 
map included as Plate VII. The data from which this map was con¬ 
structed consist of the following: 

1. Surface elevations determined for various points on the 
Hunton outcrop. 

2. Surface elevations determined for points on the outcrops 
of formations other than those belonging to the Hunton and refer¬ 
red to the top of the Hunton as a datum plane. 

3. Depths, taken from well records, at which Hunton (or 
beds easily referable to Hunton datum) were encountered. In cal¬ 
culating datum elevations from elevations on formations other than 
the Hunton the following thicknesses, for the several formations in¬ 
volved, were used; Simpson formation 1,200 feet, Viola formation 28 
500 feet, Sylvan formation l5o feet, Hunton formation 285 feet. 

ECONOMIC IMPORTANCE 

The Hunton formations are economically important in that 
they have been found to carry oil at Beebe and Maud. Faunal evi¬ 
dence indicates that the Beebe production is from the Henryhouse 
shale and possibly the Chimneyhill limestone while the oil at Maud 
is from the Bois d’Arc or Haragan. 

WOODFORD FORMATION 

NAME 

The Woodford chert was first described by Taff. 29 It presuma¬ 
bly takes its name from the town of Woodford in Carter County. 
No type section is given. 


2S In computing the restored Hunton surface elevation for the well in sec. 
16, T. 4 N., R. 4 E., a thickness of only 190 feet was used for the Viola 
limestone. This was done because of the apparent radical thinning of the 
Viola in this locality as indicated by the log of the well in sec. 20, T. 5 N., 
R. 4 E. 

29 Taff, J. A., U. S. Geol. Survey, Geol. Atlas, Atoka Folio No. 79, p. 4, 1902. 



T 2 N I T3N. 1 T4M T5N TEN 


WOODFORD FORMATION 


43 


PLATE VII 



Exposures of the formation in the Stonewall quadrangle are 
confined to two general localities. From the vicinity of Franks a 
narrow outcrop extends southeastward and, at a point about one 
mile west of the southeast corner of the quadrangle, passes out of 
the area. 

The second locality lies just to the east of the Hunton out- 


























44 


WOODFORD FORMATION 


crop on the Lawrence uplift and is exposed over an area of approxi¬ 
mately seven square miles. At its southern extremity the outcrop 
is cut off by an east-west fault so that it abuts against Pennsylva¬ 
nian (upper Boggv) strata. To the east it is succeeded by the 
Sycamore limestone, to the west by the unconformably underlying 
Hunton terrane, while to the north it passes beneath overlapping 
strata belonging to the Boggy formation. The formation is also 
exposed in several small isolated areas along the southern edge of 
the Lawrence uplift and as a small inlier in secs. 15 and 16, T. 
3 N., R. 6 E. 

THICKNESS AND CHARACTER 

Taft ' 30 gives the thickness of the Woodford as ranging from 
500 to 700 feet, but in the Stonewall quadrangle it averages much 
less than that amount. In the southeastern part of the area no sec¬ 
tions were observed with a thickness greater than 350 feet and at 
one point in sec. 22, T. 1 N., R. 7 E., a section was measured which 
totaled only 164 feet. Measurements made of the outcrop which 
occurs on the Lawrence uplift indicate that the average thickness 
there is 200 feet. 

In the southern and western parts of the Arbuckle Mountains 
the Woodford contains near its base a considerable thickness of 
cherty strata. These are apparently entirely lacking in the Stone¬ 
wall occurrences which may constitute an explanation of the les¬ 
ser thickness of the formation here. In the present investigation the 
formation was found, in the majority of cases, to consist of brown 
and black slate and shale with local bands carrying concretions of 
varying size. The greater number of concretions are round and 
about the size of a marble. Some, however, are elongate and 
variation in size up to a diameter of a foot was noted. As a rule 
the lower part of the formation is darker and more slaty than the 
upper portion. In some places the upper strata are quite shaley 
and on exposure weather to a grayish or greenish-blue color. Such 
occurrences closely resemble portions of the Caney shale. In fact, 
the general lithologic similarity of the two formations is so close as 
to make it quite difficult to distinguish between them where only 
this criterion is used. 

The very characteristic Sycamore limestone is generally pres¬ 
ent between the Caney and Woodford, however, and this with the 
rather abundant fauna of the Caney usually affords clear evidence 
as to the identity of the beds. The Sycamore limestone is quite 
thin, however, and in the consideration of well log data, where there 
is a’ strong possibility of confusing the Sycamore with other thin 
limestones such as occur in the Caney, and where faunal evidence is 


30 U. S. Geol. Survey, Geol. Atlas, Folio No. 79, 1902. 



WOODFORD FORMATION 


45 


generally lacking, it is almost impossible to distinguish the beds with 
certainty. The Woodford formation has been encountered in a 
number of wells drilled in the Stonewall quadrangle. A list of 
such occurrences is here given, but because of the difficulty just 
mentioned no attempt is made to assign accurate depths at which 
the formation was penetrated or to give its thickness in such locali¬ 
ties. The combined thickness of Caney and Woodford penetrated 
in these wells is given elsewhere. See list of well logs. 

PLATE VIII 



BLUFF OF WOODFORD FORMATION ON GOOSE CREEK. 
Location in northeast quarter of sec. 26, T. 1 N., R. 7 E. 


Wells in which Woodford has been encountered 

NE. l / A sec. 28, T. 3 N., R. 7 E. 

Center sec. 12, T. 3 N., R. 7 E. 

Center sec. 16, T. 3 N., R. 6 E. 

N. center, sec. 4, T. 4 N., R. 5 E. 

SE. cor., sec. 12, T. 4 N., R 5 E. 

NW. cor., sec. 14, T. 5 N., R. 4 E. 

M. center, sec. 20, T. 5 N., R. 4 E. 

FOSSILS 

Only a few fossils have been found in the Woodford. From 








46 


WOODFORD FORMATION 


the lower part Taff 31 reports having found a fossil tree trunk re¬ 
ferred to the Genus Dadoxylon and a small Lingula , “of the type gen¬ 
erally referred to L. spatalata”. From the upper part he reports 
two species of Productella, one of which seems referable to P. con- 
centrica Hall. In a doubtful Woodford outcrop in the Atoka quad¬ 
rangle Girty 32 found a queer form, Idiotheca rugosa, which is proba¬ 
bly an operculum of a goniatite. 

In the present investigation fossils were collected from the 
Woodford at nine localities. The numbers of these localities (see 
register of localities) are: 8a, 64, 67, 73a, 74, 131, 145, 146, and 
148. The species represented in these collections are included in 
the accompanying chart. 

AGE AND CORRELATION 

On the evidence afforded by the fossils which he collected 
Taff 33 drew the following conclusions as to the correlation of the 
formation. He says: 

This formation is of the age of the Sylamore of North Arkan¬ 
sas, the Chattanooga formation of Tennessee, the Ohio shale of 
Ohio and the Portage and Chemung of New York. At the top it 
doubtless includes strata corresponding in age with the Noel shale 
of North Arkansas and the basal shale of the Tullahoma forma¬ 
tion in Middle Tennessee. 

The evidence afforded by the larger fauna here listed is largely 
in accord with these conclusions except that the upper part of the 
formation is younger than Taff thought it to be. The form identi¬ 
fied as Proboloceras lutheri? is especially significant. Although bad¬ 
ly crushed and poorly preserved its resemblance to similarly crushed 
specimens of P. lutheri from the Portage is quite striking. Refer 
ence of the present form to this genus and species is only tentative 
since no suture lines are shown. The genus Probeloceras is restrict¬ 
ed to the upper Devonian so that it seems probable that the lower 
part of the Woodford is of that age. Specific determination of the 
Dadoxylon found has not been made, but since the genus ranges from 
Devonian to Pennsylvanian its occurrence both at the base and top 
of the Woodford is not contrary to what might be expected. 

The fauna of the upper part of the formation contains a num¬ 
ber of species common to the Moorefield, Batesville, and Fayette¬ 
ville formations of Arkansas, and together with the overlying 
Sycamore limestone and the lower part of the subsequent Caney 
formation, is thought to be at least partially equivalent to the Ar¬ 
kansas formations. Although the base of the Woodford rests un- 
conformably on the underlying Hunton terrane there is no observa¬ 
ble break within the formation. 


31 U. S. Geol. Survey, Geol. Atlas, Atoka Folio No. 79, 1902. 

32 U. S. Geol. Survey, Bull. No. 3 77, p. 40, PI. V, fig. 6, 1909. 

33 U. S. Geol. Survey, Geol. Atlas, Tishomingo Folio, No. 98, p. 5, 1903. 



Range and distribution of sfoecies in the Woodford formation 


WOODFORD FORMATION 


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X—common to the Moorfield Shale of Arkansas. 

Letters U, M, and L indicate upper, middle and lower portions of formation. 
Letters R, C, and A indicate Rare, Common, and Abundant. 


























































48 


SYCAMORE LIMESTONE 


STRUCTURE 

The structure of the Woodford conforms to that of the Hun- 
ton. See map, Plate VII. 

ECONOMIC IMPORTANCE 

At present the Woodford is not known to have any economic 
value. In wells where it has been encountered, however, it invaria¬ 
bly shows small quantities of petroleum. It is possible that locali¬ 
ties will be found where, by shooting, wells drilled into the forma¬ 
tion can be made to yield commercial quantities of oil. 

SYCAMORE LIMESTONE 

NAME 

The Sycamore limestone was named and first described by 
Taff. 34 The name is derived from Sycamore creek which crosses 
the outcrop of the formation in T. 3 S'., R. 4 E., of the Tishomingo 
quadrangle. 


AREAL DISTRIBUTION 

The Sycamore limestone has not previously been recognized 
in the Stonewall quadrangle. Its presence in the area, however, 
is now clearly established. On the Lawrence uplift the outcrop of 
the formation is definite and continuous. It forms an excellent 
reference or key horizon. Emerging from beneath overlapping, 
Boggy strata in the southeastern part of sec. 20, T. 3 N., R. 6 E., 
the outcrop extends in a general southeasterly course and enters T. 
2 N., R. 6 E., at the northwest corner of section 2. At this point 
the outcrop swings to a more easterly direction and continues to the 
eastern edge of section 12, where it turns sharply southwestward 
around the eastern end of the anticlinal axis of the Lawrence uplift. 
Within a few hundred yards to the southwest it is then cut off by 
the fault which marks the northern edge of the Franks graben. 
About one-half mile farther west, at a point just southwest of the 
cement bridge on Bois d’Arc creek, a small southwesterly-dipping 
remnant of the formation is retained in a narrow, down-drop block 
that lies between the fault just mentioned and another fault which 
passes along the southern edge of the Hunton outcrop, (here Bois 
d’Arc limestone). Another rather interesting exposure of the for¬ 
mation, also on the Lawrence uplift, is in the western part of section 
15 and the eastern part of sec. 16, T. 3 N., R. 6 E. The outcrop 
here is circular and (except at one point on its western side where 
it is overlapped by Boggy strata) continuous around a small inlier 
of Woodford. 

In the southeastern part of the quadrangle, although there are 


34 U. S. Geol. Survey, Geol. Atlas, Tishomingo Folio No. 98, p. 5, 1903. 



SYCAMORE LIMESTONE 


49 


very good exposures of the underlying Woodford and overlying 
Caney formation, the Sycamore outcrop is discontinuous and west¬ 
ward from the southeast corner of sec. 8, T. 1 N., R. 7 E., it was not 
observed. Southeast from this point to beyond Coal Creek only 
thin local outcrops were found; but in the east central part of sec¬ 
tion 22, the formation is very well exposed. Farther southeast, to 
the edge of the area, the outcrop is again poor and discontinuous. 
In the section line, on the northern slope of a hill about 150 yards 
north of a house which is located in the east central part of sec. 26 , 
T. 1 N., R. 7 E., the formation is fairly well exposed and on the 
south side of the small fault in the extreme southeastern corner of 
the quadrangle there is another good exposure. 

THICKNESS AND CHARACTER 

Taflf 35 describes the Sycamore as a lentil or wedge because of 
its increasing thickness toward the western end of the Arbuckle 
Mountains. He states that along the south side of the Mountains 
in the Tishomingo folio it is 130 feet thick. In the Stonewall 
quadrangle the formation has not been observed to have a thick¬ 
ness of more than five feet. The average, however, is less than 
this and probably does not exceed two feet. In view of the ex¬ 
treme thinness of the formation in the Stonewall quadrangle, as 
compared with the occurrence in the southern and western portions 
of the Arbuckles, it might be expected to have a considerable varia¬ 
tion in character in the two localities. This is not the case, however, 
as Taff’s original description agrees very closely with the character 
of the Stonewall exposures. For the most part the formation is a 
tough, hard limestone, slate-blue on fresh exposure, but weathering 
to a very characteristic bright yellow. Where the formation is as 
much as four or five feet thick the lower portion is generally slight¬ 
ly sandy and in some places it seems to grade laterally into shale. 
It is thought that this latter tendency explains the apparent local 
absence of the formation. Such local absence, of course, also sug¬ 
gests the possibility of a period of uplift and erosion following the 
deposition of the Sycamore. This possibility also receives support 
from the very small thickness of the formation, but in view of the 
lateral gradation into shale, especially observed in the southeast¬ 
ern part of the area, and also in view of the similarity of the faunas 
beneath and above the Sycamore, it is thought that deposition was 
continuous from late Woodford, throughout S.ycamore and into 
early Caney time. That there was a temporary change in marine 
conditions during the deposition of the Sycamore, as compared to 
what seems to have been normal conditions during the deposition of 
the Woodford to Caney inclusive, is evidenced by the variation in 


35 Loc. cit. 



50 


CANEY SHALE 


the fauna and lithologic characters of the Sycamore as compared 
with the other two formations. 

FOSSILS 

At variance with its occurrence in other portions of the Ar- 
buckle area the Sycamore limestone in the Stonewall quadrangle 
carries a fairly large fauna. A collection of fossils from locality 
number 73 was submitted to Professor Schuchert of Yale Univer¬ 
sity and was reported by him to contain the following species: 
Menophyllnm sp. Polypora sp., Productclla n. sp., Chonetes geniculatus 
White ?,Ambocoelia levicula Rowley, Brachythyris probably n. sp., Bra- 
chythyris peculiaris (Shumard)? Martinia n. sp., Composita buckleyi 
(Rowley) ? Proetus 2 species and smooth Ostracoda. 

AGE AND CORRELATION 

Professor Schuchert states (personal communication) that al¬ 
though guide forms are lacking, he is satisfied that this fauna is 
Kinderhook. In view of the Moorefield and Fayetteville-like faunas 
of adjacent portions of the Caney and Woodford formations, 
Professor Schuchert’s interpretation of the Sycamore fauna sug¬ 
gests a condition which is difficult of explanation. That is, it ap¬ 
pears that what might normally be considered a pre-Boone fauna is 
included in a formation which occurs between two other formations, 
both of which carry a fauna that might normally be considered as 
post-Boone. Ten of the thirteen species found in the upper part of 
the Woodford formation are common to the Moorefield shale of 
Arkansas and eleven are common to the Caney formation. 

As shown by Girty, 19 of the 42 species which he identified 
from the Caney also occur in the Moorefield shale, the Batesville 
sandstone, and the Fayetteville shale of Arkansas. 

Fossils in the upper Woodford and in the Lower Caney are 
more numerous and better preserved than those which occur in the 
Sycamore. 

For these several reasons, and regardless of the suggested 
Kinderhook resemblance of the Sycamore fauna, it is the writer’s 
conclusion that this formation, together with the upper portion of 
the Woodford and the lower portion of the Caney, is partially 
equivalent to the Moorefield shale, the Batesville sandstone, and the 
Fayetteville shale of Arkansas. 

CANEY SHALE 

NAME 

In common with most of the other formations of the Arbuck- 
le area the Caney shale was named and first described by Taff. 36 No 


36 Taff, J. A., U. S. Geol. Survey, Geol. Atlas Coalgate Folio No. 74, 1901. 



CANEY SHALE 


51 


type section was given. The formation presumably takes its name 
from the town of Caney which, however, is located neither on the 
Caney outcrop nor in the Coalgate sheet, but on the Missouri, Kan¬ 
sas and Texas railroad near the center of the Atoka quadrangle. 

PLATE IX. 



McALESTER-CANEY CONTACT ON SOUTH BANK OF SHEEP CREEK. 
Location near the center of sec. 1, T. 1 N., R. 6 E. Note the thin bed of 
conglomerate along the contact. 

AREAL DISTRIBUTION 

Exposures of Caney shale in the Stonewall quadrangle are 
confined to two general areas: 

1. The southeastern part of the quadrangle, and 

2. The Lawrence uplift or horst. 



52 


CANEY SHALE 


At the extreme southeastern edge of the first named locality 
the Caney outcrop extends over a broad flat area embracing about 
five square miles. In sec. 23, T. 1 N., R. 7 E., the exposure sud¬ 
denly narrows to less than one-fourth mile and from this point 
northwestward to the vicinity of Franks its width remains smah. 
Between the eastern edge of the quadrangle and the south central 
part of sec. 6, T. 1 N., R. 7 E., the upper limit of the Caney is de¬ 
fined by the next younger (Wapanucka) formation. To the west 
of the last named point Caney strata are succeeded by overlapping 
beds belonging to the upper portion of the McAlester formation. 
About one-fourth mile south of Franks the northwestward extension 
of the Caney shale terminates along the south side of a prominent 
east-west escarpment, formed by normal faulting. 

The presence of Caney shale on the Lawrence uplift was not 
recognized by either Taff or Reeds. Both of these authors map¬ 
ped its exposure there as Woodford chert. The outcrop in this 
locality is larger than that of any older formation exposed; the lower 
part is characterized by the typical fauna common to that portion 
of the formation in other localities and the general lithology is also 
in accord with that of other exposures of the formation throughout 
the Arbuckle area. 

The outcrop of the Caney shale on the Lawrence uplift extends 
in a northwest-southeasterly direction, and covers an area of ap¬ 
proximately 20 square miles. Just north of the inlier of Woodford 
formation in secs. 15 and 16, T. 3 N., R. 6 E., the northern exten¬ 
sion of the Caney is cut off by an east-west fault, while to the west 
and southwest of the inlier the formation passes beneath overlap¬ 
ping strata here assigned to the Boggy formation. Along the great¬ 
er portion of its western edge, the base of the formation is defined 
by the easily-recognizable Sycamore limestone which occurs next 
lower in the stratigraphic column. At its southern end the main 
exposure of Caney terminates against the east-west fault that sep¬ 
arates the Franks graben from the Lawrence uplift. At the east 
end of the uplift the Caney is succeeded by the Wapanucka lime¬ 
stone, and is locally overlapped by the Boggy formation. 

In addition to this main outcrop there is one much smaller ex¬ 
posure of Caney which occurs in the same general area. This is 
represented by a small down-dropped block of the formation which 
has been retained between two faults. This block is in the south¬ 
eastern part of sec. 11, T. 2 N., R. 6 E., just southeast of the cement 
bridge on Bois d’Arc Creek. The underlying Sycamore limestone 
is quite fossiliferous at this point, but no fossils were observed in the 
Caney. 


CANEY SHALE 


53 


THICKNESS AND CHARACTER 

Taff 37 states that: “On account of the level and poorly ex¬ 
posed surface of the Caney shale the structure can not be made out 
with sufficient accuracy to determine correctly the thickness of the 
formation. It is roughly estimated, however, to be 1,600 feet 
thick.” In the Stonewall quadrangle an average thickness for the 
formation is thought to be nearer 800 feet. So far as is known 
Taff’s investigations of the Caney were limited to the eastern and 
southern portions of the Arbuckle area, and it may be that the dis¬ 
crepancy which exists between the thickness which he gives for the 
formation and that observed in the Stonewall quadrangle is due to 
northward thinning such as is common with many of the other for¬ 
mations. 

In its lower portion the Caney consists of black shales and 
slates, some of which closely resemble the average strata of the 
Woodford formation. At places there occur bands of dense, blue 
limestone nodules which vary greatly as to size and shape. Such 
limestone masses sometimes attain a length of several feet and are 
usually fossiliferous. Fossils, generally goniatites, are found at the 
centers of some of the smaller masses which are probably to be 
considered as true concretions. No theory is here advanced to ex¬ 
plain the formation of the nodules. It was observed, however, that 
the shale lentils immediately adjacent to the nodules were often 
folded and crumpled, the nodules themselves not being affected. 

The upper part of the formation consists of lighter colored 
blue and greenish-blue shales, within which are interbedded occas¬ 
ional strata that are quite sandy. At one zone near the top of the 
formation sandy strata are often predominent The upper Caney of 
the Lawrence uplift is especially sandy. North of the town of 
Frisco, Caney sandstones were for a long time thought by the writer 
to represent the basal sandstones of the overlapping Boggy for¬ 
mation. Faunal evidence and structural conditions, however, prove 
them to be part of the Caney. Within the shales of the upper 
Caney there are included zones which carry either or both lime¬ 
stone concretions and limey septaria. 

FOSSILS 

The fauna of the lower part of the Caney shale has been des¬ 
cribed and figured by Girty 38 . On the accompanying chart are list¬ 
ed the 46 species and varieties of Girty’s identification as well as 29 
additional ones identified in the course of the present investigation. 
Girty’s collections were all from the lower Caney while the addi¬ 
tional species listed here are mostly from near the top of the forma- 


37 U. S. Geol. Survey, Geol. Atlas, Tishomingo Folio No. 98, p. 5, 1903. 

38 Girty, Geo. H., U. S. Geol. Survey Bull. 3 77. 



54 


CANEY SHALE 


o 


CC< 


ec 


<u 


o 

10 






CC 


pc 


cc 


cc 


a 

-o: 

Co 

c 

a 

O 

-e 


o 

a 

c 

3 

£ 


o 

"Cj< 


CO 

CO 


■:u 


ecu 


Tf 

1C 


CC oc 


w 

X 

h 


PC 


cc 


GO 

w 


fco 

a>, 

uffl (J 

few w 

HJ CU 

Z< c /2 

Q°° 

^W 

xz 

CO<; 


03 >•“ b 
0 0*8 
C > .. 

frfcS 2g 

a3 «> c 
!£0 CO o<2 c 


CO 


u 



CJ JWWUWfCWWco 


cai^:SSoooooou<:uucQCQOOO<;whh 



































































































Fauna of the Caney shale—Continued 


CANEY SHALE 


55 


c ccc 




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u jcccc 


cccc 


cccc 


xcc 


<u< 




a< 


zo ■ 

~Z£ 

1 - 1 O 

CK- 

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c/2^W 

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1£>£ 

S-Sj§| 

8*:<§a 

c " z ucc 

•i2h uw 
I-SqXX 
s^ahi- 
uu< 


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■o 2 m 

si° 

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2 2 


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rE’S 

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ija.„ 

s&gg 


to r\ « to X) C 

g u 3 q/E c • o 2 t/2 ' i<: '-— 2 ^ 

" c -coioCau,4)cecocortO 

£og««.2 MO g.5 22k£ 

g'daSS^fC’S^ o o o.2 
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<4)^0 0 0 0 O • P CO CS *-« P 

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*jC *joC 
■£ o s o 2* 

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o a 


« aj-c_2 ^ c =x)t:t 3^rga c 
tj-cj a« 2 2 § o o o 2 2« n 
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j j j 2 Z a- a- cu a, eu cu & ^ </3 h a. 


abundant. C—common. R—rare. 









































































56 


WAPANUCKA FORMATION 


tion, as exposed both in the area of the Lawrence uplift and in the 
southeastern part of the Stonewall quadrangle. 

AGE AND CORRELATION 

From the evidence afforded by the fossils the conclusion is 
here drawn that the upper part of the Caney is of Pennsylvanian 
age and partially equivalent to the Morrow formation and that 
the lower part is late Mississippian, approximately equivalent to the 
Moorefield, Fayetteville, and Batesville formations of Arkansas. 

STRUCTURE 

The structure of the Caney shale in the Stonewall quadrangle 
conforms to that of the Hunton terrane. See Plate VII. 

WAPANUCKA FORMATION 

NAME 

First described by Taff in the Coalgate folio, this formation 
supposedly takes its name from the town of Wapanucka which is 
located along the northern border of the outcrop in the Atoka 
quadrangle. Wallis 39 refers to Wapanucka as the type locality. 

AREAL DISTRIBUTION 

The Wapanucka outcrops in the Stonewall quadrangle are 
very narrow and occur in two rather widely separated localities. The 
first enters the quadrangle from the east through the central part of 
sec. 19, T. 1 N., R. 8 E., and extends northwestward for a distance 
of about six miles. In the south-central part of sec. 6, T. 1 N., R. 7 
E., it is overlapped by strata of the McAlester formation. 

Good exposures are quite numerous along this outcrop, but 
the best is at the point where the outcrop is crossed by Canyon 
Creek. 

The second exposure of Wapanucka is on the eastern end of 
the Lawrence uplift. The formation here outcrops in the south¬ 
eastern part of section 28, the northeastern part of section 3 3, 
southeastward through section 34 (all in T. 3 N., R. 7 E.) and into 
the northwestern part of sec. 2, T. 2 N., R. 7 E. Beyond the limits 
here assigned, the formation could not be traced. It is assumed that 
toward the northwest the formation passes beneath overlapping 
Boggy strata somewhere near the central part of sec. 28, T. 3 N., 
R. 7 E., and that southeastward it continues for a short distance and 
is then cut off by the east-west fault that lies iust north of Stone¬ 
wall. 


39 Wallis, B. F., Okla. Geol. Survey, Bull. No. 23, p. 30, 1915. 



WAPANUCKA FORMATION 


57 


THICKNESS AND CHARACTER. 

Wallis 40 who made a special study of the Wapanucka forma¬ 
tion, gives the following general description: 

The Wapanucka limestone consists of one or more beds of massive 
white to light brown limestone, together with chert, sandstone, and shale 
strata. Near the town of Bromide a bed of exceptionally tine, massive oolite, 
70 feet in thickness occurs. In Limestone Ridge the formation is composed 
of several members of fairly constant occurrence but variable thickness. Near 
the eastern end the strata are composed mostly of sandstone. Due to the re¬ 
sistant nature of the Strata and to the fact that the Wapanucka occurs be¬ 
tween two shale, valley-formations, the outcrops occur as narrow, steep-sided 
ridges. The formation has a variable thickness of from 100 to 800 feet, the 
average being about 300 feet. 

The Wapanucka exposed in the Stonewall quadrangle consists 
of a shale member at the base which is succeeded upward by strata 
of yellowish-white limestones, brown sandstones, and interbedded 
dark shales. 

The following sections beginning at what was considered the 
top of the formation was measured at the point in sec. 8, T. 1 N., 
R. 7 E., where Canyon Creek crosses the outcrop: 

Section of Wapanucka formation. 

Feet 


Yellowish-white limestone Very fossiliferous_-13 

Shale__3 0 

Yellowish white limestone -- 5 

Shale with thin layers of limestone- 50 

Oolitic limestone- 3 


Blue and gray-blue calcareous shale. Very fossiliferous 50 


151 

That the Wapanucka has a greater downward extension than 
is here given, and that all the underlying strata which have been re¬ 
ferred to the upper or Pennsylvanian Caney are in reality to be con¬ 
sidered a part of the Wapanucka is suggested by the position of the 
oolite which occurs only 50 feet above the base of the Canyon 
Creek section. In the region to the southeast, beyond the limits of 
the Stonewall quadrangle, an oolitic member of the Wapanucka be¬ 
comes quite prominent. On Delaware Creek near Bromide it has 
a thickness of 70 feet. Speaking of this member Wallis 41 says: 
“the oolite is to be considered as a local phase of the massive lime¬ 
stone member that occurs at the top of the formation.” In the 


40 Idem. p. 30. 

41 Idem. p. 77. 









58 


WAPANUCKA FORMATION 


Canyon Creek section, however, the yellowish-white limestone 
which occurs 83 feet above the oolite carries a characteristic Wap- 
anucka fauna. From the evidence thus afforded, the conclu¬ 
sion is drawn, that the oolitic members of the two localities are not 
the same, the Canyon Creek stratum being lower in the formation 
than the one at Delaware Creek. 

The shale at the bottom of the Canyon Creek section has a 
lithologic appearance somewhat similar to that of the underlying 
Caney, but the two were easily distinguished by the following fea¬ 
tures: 

1. The basal shale of the Wapanucka carries a very prolific fauna which is 
characteristic of the formation. 

2. The Caney shale is less calcareous and slightly the darker of the two, 
also it is often more sandy. 

3. The upper part of the Caney shale, although fossiliferous and although 
carrying a fauna somewhat similar to that of the Wapanucka—in that 
they are both Pennsylvanian—has a barren zone of some 60 feet at its 
upper limit. 

4. Ironstone concretions, characteristic of the upper Caney, occur in this 
barren zone. 

5. The fauna of the fossiliferous portion of the upper Caney has only a few 
forms which are common to the Wapanucka formation. * 

Wallis 42 observed unconformities at the bottom, top, and 
within the Wapanucka limestone. At Delaware Creek in sec. 9, 
T. 2 S., R. 8 E., he noted a limestone breccia at the top of the for¬ 
mation. He states that: 

This breccia is composed of highly angular fragments of a very dense 
light gray to white limestone similar in appearance to the Arbuckle lime¬ 
stone. . . . There are also present fragments of an oolite which is very dif¬ 
ferent from the Wapanucka oolite proper. . . The oolite found in the brec¬ 
cia may be of Chimneyhill age or may belong to another formation (Viola or 
Arbuckle limestone) the oolitic character of which, due to the fine grain of 
the rock, has been overlooked. 

Definite evidence of unconformities within the Wapanucka for¬ 
mation in the Stonewall quadrangle was not secured. The fact that 
the oolite mentioned in the Canyon Creek section was found only in 

42 Idem. pp. 69-72. 

*_Note: After completing a study of the Caney and Wapanucka faunas it 
appears that it would be desirable to restrict the term Caney to the Miss- 
issippian part of the formation and to describe as a new formation the upper 
or Pennsylvanian part. Time, however, is not available to make the 
necessary changes in mapping so that this undertaking will have to be left 
to the future. 



WAPANUCKA FORMATION 


59 


that one locality may, however, be considered as indicative of an 
unconformity at that horizon. 

Above the yellowish-white limestone placed at the top of the 
Canyon Creek section there is a dark shale which, except for one 
sandstone (four feet thick) 45 feet above its base, has but little lith¬ 
ologic variation through 125 feet. The base of this shale is taken 
as the contact between the Wapanucka and the overlying Atoka 
formation. 

Less is known of the Wapanucka where it outcrops on the 
Lawrence uplift. In the original mapping the beds there were as¬ 
signed to the overlapping Boggy formation. Subsequent faunal 
studies, however, indicated the presence of the formation and at 
the writer’s request Mr. A. E. Brainerd kindly returned to the area 
and made several large collections. The collections contain a typ¬ 
ical Wapanucka fauna and there can be no doubt that the forma¬ 
tion outcrops in the area described. The limestones are somewhat 
darker than is typical of such beds in the Wapanucka where the 
formation is exposed farther south. Waterworn pebbles of slate, 
chert, and limestone also occur in the limestones. The pieces of 
slate are more abundant than either the chert or limestone pebbles; 
the latter being small and very rare. Such conglomeratic strata 
were not found in the Wapanucka where it outcrops in the south¬ 
eastern part of the Stonewall quadrangle, but they recall the con¬ 
glomerate noted by Wallis 43 at the top of the formation in the 
Atoka quadrangle. 

The difference in the conglomeratic strata in the two local¬ 
ities is suggestive. Wallis described the conglomerate at Dela¬ 
ware Creek (sec. 9, T. 2 S., R. 8 E.) as a “breccia . . . composed of 
highly angular fragments of a very dense, light-gray to white lime¬ 
stone similar in appearance to the Arbuckle limestone.” He also 
noted within it fragments of oolite which differ from the Wap¬ 
anucka oolite proper, and which he believed to have been derived 
from the Chimneyhill, Viola, or Arbuckle limestone. The pebbles 
in the Wapanucka strata of the Lawrence uplift are small, water- 
worn, and consist of material all of which might have been derived 
from the Caney and Woodford formations. 

From this comparison it appears that at the time the Wap¬ 
anucka was being deposited the limestones of the Arbuckle Moun¬ 
tains were exposed in the vicinity of the Delaware Creek area, but 
that farther north they were concealed by the overlying Caney and 
Woodford formations. 

The thickness of the Wapanucka formation on the Lawrence 
uplift is thought to be less than 100 feet. 


43 Wallis, B. F., Okla. Geol. Survey, Bull. 23, p. 71, 1915. 



60 


WAPANUCKA FORMATION 


FOSSILS 

The species listed on the accompanying chart were secured 
from the several collections taken. 


AGE AND CORRELATION 

The Wapanucka fauna contains several species which are nor¬ 
mally confined to the Mississippian. The Pentremites especially 
exemplify this. The majority of species, however, are typically 
Pennsylvanian and on the evidence which they afford the formation 
is unhesitatingly assigned to the Pennsylvanian. Further proof of 
the Pennsylvanian age of the Wapanucka is also afforded by the still 
older and even more typical Pennsylvanian fauna in the upper por¬ 
tion of the Caney shale. 

The close similarity of the Wapanucka fauna and that of the 
Morrow formation of Arkansas and northeastern Oklahoma, as de¬ 
scribed by Mather, 44 obviates the necessity of discussion. The two 
formations are at least partially equivalent. The number of species 
common to the Marble Falls formation of Texas also assures a cor¬ 
relation in that direction. In the publications of Taff, Reeds, and 
Wallis the Wapanucka was correlated with the so-called Franks con¬ 
glomerate which is exposed near the town of Franks. As shown 
elsewhere, 45 however, this correlation is not well founded, the 
Pennsylvanian strata exposed near Franks representing the shore¬ 
ward phase of the McAlester, Savanna, Boggy, and younger strata 
including the Francis formation. 

STRUCTURE 

Throughout both its outcrops in the Stonewall quadrangle the 
normal dip of the Wapanucka formation is toward the northeast. 

ECONOMIC IMPORTANCE. 

The Wapanucka of the Stonewall quadrangle will probably 
never be of commercial importance. Farther southeast, however, 
the oolitic phase yields building stone which is said to be of excellent 
quality. The economic importance of the Wapanucka formation 
has been discussed in detail by Wallis. 46 

44 Maiher, K. F., Bull. Denison Univ., vol. 18, p. 59, 1915. 

45 Morgan, Geo. D., Okla. Geol. Survey, Circular No. 12, 1923. 

46 Loc. Cit. 



WAPANUCKA FORMATION 


61 


Fauna of the Wapanucka formation 


SPECIES 

19 

23 

LOC^ 

28 

lLITII 

37 

3S 

41 

170A 

ANTHOZOA 







Cladochonus fragilis. . 



C 




Cyathaxonia sp. 

R 

C 

C 

C 



Lophophyllum profundum . 


C 

A 

A 

A 

R 

Micheienia eugeneae. 


A 

A 

A 


Michelenia subcylindrica. 

R 


R 

R 

A 

R 

Tiiplophyllum sp. 



C 


R 

BLASTOIDF.A 







Pentremites angustus. 

R 

R 

A 

A 

R 

R 

Pentremites rusticus....... 




C 



CRINOIDEA 







Agassizocrinus conicus. 

R 

R 

C 

R 


R 

Ceriocrinus hemisphericus.... 


R 




Eupachycrinus magister..._. 

A 

R 

A 

C 



Hydrcioncrinus sp.... ... 

R 






Stereobrachicrinus pustulossus.. 

R 






ECHINOIDEA 







Archaeocidaris sp. . 

R 





R 

BRYOZOA 






Cvstodyctia brentwoodensia 



R 




Fenestella mimica. 


R 





Fenestella sevillensis...... 



R 




Fenestella venusta. 

R 






Glyptopora crassistoma. 


R 

R 




Glyptopora incrustans n. sp...... 


R 





Polypora cestriensis..... 


R 





Polypora spinulifera.... 


R 





Rhombopora lepidodendroides 



R 




Rhombopora persimilis . .. 



R 




Rhombopora snideri... 



R 




Stenopora bullata n. sp.. 



R 




Stenopora circina n. sp..... 



R 




Stenopora hispida n. sp. . 



R 




Stenopoar micropora, n. sp. 



R 




Stenopora tuberculata... 



R 




Stenopora wapanuckensis n. sp.. 



R 




BRACHIOPODA 







Chonetes granulifer .... 



R 




Chonetes laevis .. 



R 




Composita arkansanum...... 


R 


R 

c 


Gomposita deflecta . 



R 

A 


R 

Composita gibbosa .. 



R 


c 

Composita ovata. 



R 




Composita ozarkana.. ..... 


A 

R 




Composita subtilita.. 


C 





Composita wasatchcnsis .... 



C 

c 



Derbya crassa ...... 


A 

R 

A 



Dielasma subspatulatum __ 

R 

R 





Hustedia brentwoodensis .. 



R 


R 

c 

Hustedia miseri __ 


R 

C 

A 

R 

C 

Hustedia mormoni... . ..... 





R 

Orbiculoidea sp.... 

R 






Productussp. . ________ 

R 






Productus cora .. 



A 

R 


R 

Productus gallatinensis ... 




R 

R 


Productus gallowayi n. sp..... 




A 



Productus morrowensis... 





R 



A—abundant. C—common. R—rare. 











































































































































































































62 


WAPANUCKA FORMATION 


Fauna of the Wapanucka formation—Continued 


BRACHIOPOD A—Continued 


Productus nanus. 

Productus welleri. 

Pustula bullata... 

Pustula nebraskensis. 

Pustula punctata.... 

Rhipodomella altirostris. 

Rhynthopora magnicosta.... 
Schizophoria resupinoides—. 

Spirifer cameratus. 

Spirifer goreii. 

Spirifer opimus. 

Spirifer rockymontanus.. 

Spiriferina campestris .... 

Spiriferina kentuckyensis.... 

Spiriferina transversa...... 

Squamularia transversa.. 


PELECYPODA 


Astartella concentrica. 

Astartella varica ... 

Aviculopecten halensis. .... 
Aviculopecten occidentalis. 

Conocardium sp. 

Leda bellistriata.....1. 

Myalina sp. 

Nucula sp. 

Nucula parva..—. 

Schizodus cf. morrowensis.. 
Solenomya sp. 


TRILOBITA 


Griffithides morrowensis 
Griffithides sp. 


GASTROPODA 


Euphemus carbonarius. 

Schizostoma catilloides. 

Meekospira sp. 

Phanerotrema grayvillense ... 

Platyceras parvum....... 

Pleurotomaria missouriensis 

Sphaerodoma sp. 

Worthenia tabulata. 

Zygopleura ? sp. 


CEPHALOPODA 


Gastrioceras angulatum. 
Gastrioceras pygmeum... 
Orthoceras tuba.. 


19 


R 

R 


R 


23 


A 

A 

A 

G 

A 


R 

C 

A 


R 

R 


G 

R 

C 

R 


R 


R 


R 


28 


C 

C 


R 


A 

A 


A 

R 


R 


R 


R 


R 


R 

9 


37 


A 

R 

R 

R 

R 

A 


R 

R 

R 


R 


R 


R 


R 


41 


R 

R 


R 


R 


R 


R 


Px 

R 


R 


170 A 


R 

R 


R 


R 


R 


A—abundant. C—common. R—rare. 


ATOKA FORMATION 

NAME 

The town of Atoka is situated on the outcrop of this forma¬ 
tion. Taff and Adams 47 who named and described the formation, 


47 U. S. Geol. Survey, 2lst Annual Report, Part 2, p. 273, 1900. 







































































































ATOKA FORMATION 


63 


however, do not mention Atoka as the type locality and it is only 
conjectural that the formational name is derived from that of the 

town. 

AREAL DISTRIBUTION 

In the Coalgate and Atoka folios to the east and southeast, 
respectively, of the Stonewall quadrangle, the outcrop of the Atoka 
formation is very broad. Along the western edge of the Coalgate 
quadrangle, however, the outcrop suddenly narrows from a width 
of more than three miles to less than one-half mile. In its ex¬ 
tension northwestward into the Stonewall quadrangle the narrow 
width of the exposure is maintained, gradually becoming less, until 
at a point a few hundred yards west of Canyon Creek it is com¬ 
pletely overlapped by the upper beds of the McAlester formation. 

THICKNESS AND CHARACTER 

The Atoka consists of alternating sandstones and shales with a 
few impure limestones near its base. The latter are to be observed 
on Canyon Creek, a short distance north of the Wapanucka out¬ 
crop. A chert bed known as the Chickachoc chert lentil occurs 
in the lower part of the formation where it outcrops in the southern 
part of the Coalgate and the northern part of the Atoka quad¬ 
rangle. This chert lentil was not observed in the Stonewall ex¬ 
posure. Taff mentions another type of strata which occurs within 
the Atoka formation. In describing these beds he says: 

Prominent local beds of conglomerate composed of fine brown sand and 
sub-angular chert pebbles make high ridges and hills immediately west and 
southwest of Stringlown. Conglomerate beds of similar nature occur also 
in the upper part of the formation west of North Boggy Creek and north and 
west of Atoka. A peculiar feature of this chert conglomerate is that its 
limit in range north and south corresponds with the occurrence of Silurian 
chert [mapped as Talihina Chert] in Black Knob Ridge. 

These conglomerates are important in that others of a very 
similar character are common in practically all the formations later 
than the Atoka which are present in the Stonewall quadrangle. 
Their greatest development, however, is in the formations above the 
Wetumka shale. 

The thickness of the Atoka in the Coalgate and Atoka quad¬ 
rangles, as given by Taff in the folios covering those areas, is 3,000 
feet. In the Stonewall area, however, the exposed section is very 
much less and is estimated to be only 800 feet. On the geological 
maps of the Coalgate folio the abrupt narrowing of the outcrop, 
with a similar apparent decrease of section, at the western edge of 
the quadrangle is interpreted as a possible result of faulting. The 
east-west fault which is dotted-in on the folio maps, if extended 
westward, would enter the Stonewall quadrangle through the north¬ 
ern part of sec. 19, T. 1 N., R. 8 E. just north of the Wapanucka 


64 


ATOKA FORMATION 


outcrop. Although the strata at this point dip very steeply toward 
the north, no conclusive evidence of faulting could be found. In 
the absence of such evidence it is thought that the narrower outcrop 
and lesser thickness of the Atoka formation in the Stonewall quad¬ 
rangle, as compared with the region to the east, may be explained 
more logically and confidently in a different manner. 

Extending in a north-south direction along the western edges 
of secs. 24 and 25, T. 1 N., R. 8 E.,in theCoalgate quadrangle, there 
is a very sharp anticline in the Atoka formation. If this fold is follow¬ 
ed northward to the center of section 23 it is found to pass beneath 
the undisturbed outcrop of the Hartshorne sandstone. This sug¬ 
gests that the Atoka formation was uplifted, folded, and peneplaned 
before the Hartshorne sandstone was deposited. If the validity of 
this interpretation is assumed, the Hartshorne sandstone represents 
an overlapping formation which was laid down across the beveled 
edges of the underlying Atoka formation. With subsequent uplift 
and erosion it is only natural that the mantle of Hartshorne and suc¬ 
ceeding beds would be removed differentially from the Atoka. Thus, 
in certain localities where the Hartshorne was but slightly folded a 
large part of the Atoka would be exposed while at others where the 
dip was steep only the basal part of that formation would be un¬ 
covered. In other words it is thought that the thin section and 
narrow outcrop of the Atoka formation in the Stonewall quadrangle 
probably result from the concealment of the upper part of the for¬ 
mation by the overlapping Hartshorne sandstone. As previously 
stated the Atoka outcrop is completely concealed a short distance 
west of Canyon Creek by overlapping strata of the upper McAlester 
formation. 

FOSSILS 

Within the Stonewall quadrangle no fossils were found in the 
Atoka formation. In the western part of the Coalgate quadrangle 
two small collections yielded the following species: 

Northeast corner sec. 26, T. 1 N., R. 8 B., from westward 
dipping limey sandstone. 

Rhombopora sp. 

Derbya crassa? 

Composita subtilita 
Spirifeiina kentuckyensis 
Squamularia? transversa 
Hustedia mormoni 
Spirifer cf. cameratus 
Dielasma subspatulatum 
Schizodus sp. 

Bellerophon sp. 

Phillipsia? sp. 


HARTSHORNE SANDSTONE 


65 


Central part sec. 20, T. 1 NR. 8 /row northward dipping sand¬ 
stone strata. 


Fish tooth 

Schizodus cf. meekanus 
Allorisma terminale 
Pharkidonotus percarinatus 
Gastropod trails 

AGE AND CORRELATION 

The meager fauna is not sufficient to justify any attempt to 
correlate the Atoka with definite formations of other regions. The 
forms listed all have a rather long range; they are, however, all 
common to the early Pennsylvanian. In the absence of any species 
indicative of a later age and on the evidence afforded by the faunas 
of higher and lower formations, it seems probable that at least the 
lower part of the Atoka is of Pottsville age. 

STRUCTURE 

Atoka strata exposed in the Stonewall quadrangle dip steeply 
in a direction slightly east of north. 

ECONOMIC IMPORTANCE 

The formation is not known to have any special economic 
value. In areas of favorable structure some of its strata might yield 
commercial quantities of oil or gas. 

HARTSHORNE SANDSTONE 

NAME 

The name of this formation is after the town of Hartshorne, 
situated in the eastern part of the McAlester quadrangle. Taff, 48 
who first described the formation gave the name in 1899. 

AREAL DISTRIBUTION 

The Hartshorne sandstone in the Stonewall quadrangle is with 
difficulty distinguished from the overlying McAlester and the under¬ 
lying Atoka formations. The limits are indefinite and preclude the 
possibility of accurate mapping. From the western edge of the 
Coalgate quadrangle, to which point the formation was mapped by 
Taff, there is a continuation into the Stonewall quadrangle of sev¬ 
eral brown sandstones with interbedded shales. This group of strata 
resists erosion somewhat better than the more shaley beds above and 
below it and for that reason is generally expressed as a low, rounded 
ridge. It is thought that these strata represent the westward exten¬ 
sion of the Hartshorne sandstone and they have been so mapped. 


48 Taff, J. A., U. S. Geol. Survey, 19th Ann. Rept. Pt. 3, p. 436. 



66 


HARTSHORNE SANDSTONE 


The ridge formed by the formation crosses the eastern line of 
sec. 13, T. 1 N., R. 7 E., just one-fourth mile north of the southeast 
corner of the section, and continues westward and southwestward in¬ 
to the northeast corner of section 23. At the latter point the ridge 
dies out, but with the turn of the outcrop toward the northwest, it 
again appears in the southern part of section 14 and continues 
along the south side of Coal Creek almost to the point where that 
stream crosses the outcrop in the eastern part of section 15. From 
the crossing of Coal creek northwestward the limits of the forma¬ 
tion could be located only approximately. In the south part of sec. 
9, T. 1 N., R. 7 E., the Hartshorne sandstone is completely overlap¬ 
ped by the upper part of the McAlester formation. 

THICKNESS AND CHARACTER 

Farther east the Hartshorne sandstone has a thickness of as 
much as 200 feet, but in the portion of its outcrop here discussed 
the formation is only about 100 feet thick. It consists of brown or 
yellowish-brown sandstones with interbedded shales. 

FOSSILS 

No fossils were found in the Hartshorne sandstone. 

AGE AND CORRELATION 

In the absence of fossils no definite evidence can here be con¬ 
tributed as to the age or correlation of the Hartshorne sandstone. 
From the roof shales of a coal bed (Hartshorne or Grady Coal) 
which occurs only a short distance above the Hartshorne formation, 
White 49 indentified a number of plant fossils. From the evidence 
thus afforded he concluded that the coal bed in question, “is refer¬ 
able to the Lower Productive Coal Measures (Allegheny series) of 
the northeastern bituminous fields, its stage being probably near the 
middle of that series, and presumably in the lower half.” 

The close association and apparent conformity of this coal 
with the Hartshorne sandstone indicates that the two are of similar 
age and that the Hartshorne sandstone is likewise to be assigned to 
the lower part of the Allegheny series. 

In computing the average maximum range and percent of 
common species of the fossils of the strata of the Stonewall quad¬ 
rangle, as compared with those of adjoining regions, the lack of 
fossils in the Hartshorne sandstone operates to assign it a position 
below the Cherokee of Kansas and Missouri, and to make it equiv¬ 
alent to a part of the Millsap of Texas. This is in accord with the 
correlation of the overlying McAlester formation. 


49 White, David, U. S. Geol. Survey 19th Ann. Rept. Pt. 3, p. 468, 1899. 



McALESTER FORMATION 


67 


STRUCTURE 

In the Stonewall quadrangle the direction of average dip of 
the Hartshorne sandstone is slightly east of north. 

ECONOMIC IMPORTANCE 

Near the town of Hartshorne this formation carries near its 
top a workable coal bed. This bed was not observed in the Stone¬ 
wall area. 


McALESTER FORMATION 

NAME 

Next above the Hartshorne sandstone is the McAlester forma¬ 
tion. It was named and first described by Taff in Part III, of the 
19th Annual Report of the United States Geological Survey. The 
name is presumably after the town of McAlester, located in the 
north central part of the McAlester quadrangle. No specific type 
section was given. 

AREAL DISTRIBUTION 

In the Stonewall quadrangle the outcrop of this formation has 
an average width of less than one-half mile. Its lateral extent is a 
little over seven miles along a northwest-southeast strike. The 
outcrop enters the area through the central part of sec. 18, T. 1 N., 
R. 8 E., and terminates against a normal fault just south of the town 
of Franks. 


THICKNESS AND CHARACTER 

In the McAlester district and in the eastern part of the Coal- 
gate quadrangle, the McAlester formation is reported 50 to have a 
thickness of nearly 2,000 feet. It thins toward the west, however, 
and in the western part of the Coalgate quadrangle is said by Taff 
not to exceed 1,500 feet. A section made along the east line of 
the Stonewall quadrangle gave a total of only a little more than 
1,000 feet for the formation, while farther west the thickness grad¬ 
ually decreases to only a few hundred feet. 

In describing the geology of the McAlester district Taff 51 
divides the McAlester formation into three parts of which he says: 

The lowest one is composed almost entirely of shale, with thin sand¬ 
stone and coal, in all 800 feet thick. . . . The Hartshorne or Grady coal 

occurs at the base of this shale. The middle division.is composed of 

three or four beds of sandstone separated by shale 100 feet to 200 feet thick. 

50 Taff, J. A., U. S. Geol. Survey 19th Annual Report, Pt. 3, 1899, and U. S. 

Geol. Survey, Geol. Atlas Coalgate Folio No. 74, 1901. 

51 U. S. Geol. Survey 19th Rept. Pt. Ill, p. 437, 1899. 




68 


McALESTER FORMATION 


Together these beds of sandstone and shale are about 500 feet thick. . . . The 
upper division is almost entirely of shale nearly 700 feet thick and the Mc- 
Alester coal is about 5o feet above its base. 

In the Coalgate folio, as mentioned above, Taflf directs atten¬ 
tion to the westward thinning of the formation and further states 
that in this area there are two coal beds in the McAlester formation; 
one at the base and the other about 200 feet below the top. The 
higher of these beds is known as the Lehigh Coal and is to be dis- 

PLATE X 



A. LEHIGH COAL BED AS EXPOSED IN THE STRIP-PIT 
SEC. 14, T. 1 N., R. 7 E. 

tinguished by a black, bituminous shale, about 18 inches thick, 
which forms the roof of the coal and which carries an abundance 
of molluscan shells, and the teeth and scales of fish. In the south¬ 
eastern part of sec. 14, T. 1 N., R. 7 E., about 200 feet below the 
top of the McAlester shale, is a strip pit (Plate X) from which 
the Lehigh coal is mined. The characteristic roof shale is here very 
well exposed. The coal and overlying shale are again well exposed 



McALESTER FORMATION 


69 


on the north bank of Coal Creek in the eastern part of sec. 15, T. 
1 N., R. 7 E., where that stream turns sharply toward the east. The 
lower Hartshorne or Grady, coal was not found in the Stonewall 
quadrangle and is thought to be covered by overlapping strata. 

In its Stonewall exposure the upper part of the McAlester con¬ 
sists very largely of dark colored shales which, however, carry a 
few thin beds of sandstone. In the portion below the coal, sand¬ 
stone is prominent, but even here the strata consists largely of shales. 
The most important bed, geologically, in the McAlester formation 

PLATE X. 



B. GENERAL VIEW OF STRIP-PIT IN SEC. 14, T. 1 N., R. 7 E. 


is a thin red limestone which occurs 15 feet below the Lehigh Coal. 
This bed was traced almost continuously along the outcrop mapped 
in the present survey and contributes quite conclusive evidence as 
to the relation of the McAlester with the formations above and be¬ 
low it. Where the red limestone outcrops just south of the strip 
pit in section 14, it is approximately 2,000 feet above the Wapa- 
nucka limestone, but at its last observed western exposure, along 
the eastern edge of sec. 1, T. 1 N., R. 6 E., it is only 465 feet above 
the Caney shale; the Wapanucka, Atoka and Hartshorne formations 
being there absent. This condition is taken to indicate (1) that 





70 


McALESTER FORMATION 


the McAlester is an overlapping formation; (2) that the top over¬ 
laps the base, probably thus accounting for at least a part of the 
supposed westward thinning mentioned by Taff; and (d) that in 
the Stonewall quadrangle the overlap of the upper part of the for¬ 
mation continues to such an extent that it projects across the bev¬ 
eled edges of older formations and, in the region just south of 
Franks, rests on the Caney shale. (See Plate lx.) 

In its western extent the exposed portion of the McAlester 
formation carries numerous beds of conglomerates. On the west 
bank of Canyon Creek there is such a stratum which rests uncon- 
formably on limestone beds of the lower part of the Atoka forma¬ 
tion. This conglomerate is largely composed of reworked frag¬ 
ments from the Caney and Woodford formations, but also carries 
a few pieces of the uppermost, exposed limestone of the Atoka. 
The absence from the conglomerate of fragments of Arbuckle strata 
older than the Woodford suggests that the older formations were 
not exposed in the immediate vicinity at the time the conglomer¬ 
ate was deposited. The importance of this observation lies in the 
fact that in the Atoka quadrangle, at a point some 15 miles to the 
southeast of the Canyon Creek locality, Wallis 52 found at the 
top of the Wapanucka formation a conglomerate which carried frag¬ 
mental limestone very similar to that of the Viola and Arbuckle for¬ 
mations. The natural conclusion, therefore, is that the Arbuckle 
Mountains were first uplifted at some point to the south of their 
present highest portion. This conclusion is substantiated by the 
fact that at the southeastern edge of the mountains all of the thick 
section of early Paleozoic rocks has been removed, thus exposing 
granite, while in the area just south of the point at which the Mc¬ 
Alester conglomerate bed is exposed in Canyon Creek, several thou¬ 
sand feet of these older rocks are still present above the granite. 

Farther west, later conglomerates in the McAlester carry frag¬ 
ments of Hunton limestone and numerous well preserved specimens 
of Camarocrinus which were very probably derived from either the 
Henryhouse or Haragan shales. The red limestone which occurs 
below the Lehigh Coal also becomes more clastic westward and 
just north of the road and house, one-half mile south of the NW. 
cor. of sec. 6, T. 1 N., R. 7 E., contains limestone pebbles up to an 
inch in length. Fragments of coal were also observed in the lime¬ 
stone at this place. The conglomerates in the western extension of 
the McAlester formation were included by previous workers as part 
of the Franks conglomerate. 

FOSSILS 

The fauna of the McAlester formation, as determined from 
several collections all taken from localities within the Stonewall 


52 Wallis, B. F., Okla. Geol. Survey, Bull. No. 23, p. 71, 1915. 



McALESTER FORMATION 


71 


quadrangle, is shown on the included chart. 

AGE AND CORRELATION 

The following suggestions regarding the age and correlation of 
the McAlester formation are given in the literature. White 53 states 
that it is probable that the McAlester coal ,near the top of the for¬ 
mation, represents a horizon in the lower part of the Missourian, 
later than the Bethany limestone. 

Bloesch 54 thinks that the Hartshorne, McAlester, and Savanna 
formations are equivalent to the Winslow formation of Arkansas 
and northeastern Oklahoma. McCoy 55 states that “The Blue¬ 
jacket sandstone of eastern Oklahoma which outcrops just west of 
Pryor, Oklahoma, has been traced south and southeast and mapped 
by E. A. Trager, W. R. Berger, F. L. Aurin, and D. K. Greger as a 
sandstone near Warner, Oklahoma which occurs in the lower por¬ 
tion of the McAlester shale in eastern Oklahoma. A small trilo- 
bite horizon, about 70 feet below the Bluejacket sandstone near 
Pryor was found below the Warner sandstone in several places and 
this zone was estimated by Aurin to be 150 feet above the top of 
the Hartshorne sandstone.” 

In McCoy’s 56 opinion the McAlester formation is equivalent 
to a lower portion of the Cherokee shale of Kansas. 

Plummer 57 and Moore are of the opinion that the McAlester 
is probably to be correlated with the Mineral Wells formation of 
Texas. 

The faunal evidence gathered in the present work leads to the 
conclusion that the upper part of the McAlester formation is equiva¬ 
lent to the lower part of the Mineral Wells formation of Texas and 
to the lower Cherokee of Kansas and Missouri. The lower part 
of the formation is correlated with the upper Millsap of Texas and 
is below the Cherokee of Kansas and Missouri. 

STRUCTURE 

In its exposure southeastward from Franks to the edge of the 
quadrangle the McAlester formation dips at angles which vary from 
two or three to as much as 40 degrees. The direction of dip is nor¬ 
mally about north 40 degrees east. 

In the east central part of sec. 8, T. 1 N., R. 7 E., a small fault 
crosses the outcrop. The direction of this fault is northeast-south¬ 
west; its displacement is approximately 50 feet and the upthrown 
side is toward the west. 

53 White, David, U. S. Geol. Survey 19th Ann. Rept. Pt 3, p. 464,1899. 

54 Bloesch, Edward, Amer. Assn. Pet. Geol. vol. 3, p. 269, 1919. 

55 McCoy, Alex. W., Am. Assn. Pet. Geol. vol.. 5, p. 548, 1921. 

56 Idem. p. 549. 

57 Plummer, F. B., and Moore, R. C., Univ. of Texas, Bull. No. 2132, p. 209, 

1921. 



LOCALITIES 


72 


McALESTER FORMATION 


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Fauna oj ihe McAtesier jormation—Continuea 


McALESTER FORMATION 


73 



_abundant. C—common. R—rare 


















































































74 


SAVANNA SANDSTONE 


ECONOMIC IMPORTANCE 

In the Stonewall quadrangle the only economic importance of 
the McAlester formation is that afforded by the Lehigh coal which 
is mined on a small scale at the strip pit in sec. 14, T. 1 N., R. 7 E. 
(See Plate X—A and B) 

SAVANNA SANDSTONE 

NAME 

Next above the McAlester formation is the Savanna sandstone. 
It is presumed that the name of this formation is derived from the 
town of Savanna located in the McAlester quadrangle. Taff 58 , how¬ 
ever, who gave the name and who first described the formation, 
does not explain the derivation of the term neither does he define a 
type section. 

AREAL DISTRIBUTION 

In the vicinity of Jesse the Savanna outcrop has a width of 
two miles. South of the westward-plunging syncline, which occurs 
in section 11 south of this town, the outcrop rapidly narrows and 
in its continuation toward the northwest the average width is only 
about one-half mile. The formation is cut off to the northwest by 
the east-west fault which is marked by the escarpment just south of 
Franks. The total areal extent of the formation in the Stonewall 
quadrangle is approximately seven square miles. 

THICKNESS AND CHARACTER 

A section measured along the east line of T. 1 N., R. 7 E., shows 
a thickness of Savanna amounting to approximately 1,300 feet. 
Westward, however, the exposed portion of the formation is great¬ 
ly decreased because of the combined effect of two overlaps. A 
section measured about two miles southeast of Franks shows only 
400 feet of Savanna. 

The formation consists of alternating shales and sandstones, 
with occasional thin, impure limestones. Toward the western end 
of the outcrop conglomeratic beds become prominent. These car¬ 
ry fragments of oolitic and pink-crinoidal limestone from the Chim- 
neyhill formation. Other limestone fragments included in the con¬ 
glomerates closely resemble strata from the Viola and Arbuckle. 
The conglomeratic phase is a part of the Franks conglomerate of 
previous investigators of the Arbuckle area. 

JOLLY LIMESTONE MEMBER 

Near the bottom of the Savanna there is a thin limestone bed 
which is important in that it shows clearly the overlapping nature 


58 U. S. Geol. Survey 19th Annual Report, Part 3, p. 437, 1899. 



SAVANNA SANDSTONE 


75 


of itself, and the strata above it, across the basal beds of the forma¬ 
tion. This bed is very well exposed in the road in front of J. S. 
Jolly’s house, 300 yards east of the northwest corner of sec. 8, T. 

} N., R. 7 E. It carries an abundant gastropod fauna, the most prom¬ 
inent species of which is Bellerophon crassus var. zvewokanus. At 
the point just mentioned the limestone is less than 100 feet above 
the top of the McAlester formation. When followed southeastward 
to the west side of section 10 of the same township and range it is 
found to swing toward a more easterly direction, while the strike 
of underlying strata continues southeastward. In this way a greater 
and greater section is exposed between the diverging outcrops until 
in the area near the eastern edge of the outcrop the limestone in 
question is approximately 200 feet above the top of the McAlester 
formation. 

Except at the eastern edge of the area it was found to be im¬ 
possible to draw the contacts of the Savanna formation with ac¬ 
curacy. The entire formation and the succeeding Boggy formation, 
although themselves separated by an unconformity, constitute a pro¬ 
gressively overlapping series. At the eastern edge of the area there 
is, at the base of the formation, a series of sandstones which can be 
followed westward without difliculty about two miles. These beds 
then lose their prominence. In strike with them, however, and at 
a fairly uniform but gently decreasing interval above the red lime¬ 
stone under the Lehigh coal there is an escarpment which is thought 
to represent their westward extension. In the southeastern part of 
sec. 9, T. 1 N., R. 7 E., the escarpment dies out. Thin beds exposed 
at this terminus are about 100 feet below the Jolly limestone mem¬ 
ber of the Savanna and for that reason the base of the formation, 
from this point westward, is taken as being about 100 feet below the 
limestone bed. 

At the western edge of the Coalgate quadrangle the top of thr 
formation is limited by a sandstone which is succeeded by the basal 
shale of the Boggy formation. Westward the Boggy strata swing 
around and across the Savanna. The problem of mapping is ad¬ 
ditionally complicated by the fact that successively higher beds in 
the Boggy are progressively overlapping. Without spending more 
time on the problem than was available in the present investiga¬ 
tion it would perhaps be better not to attempt a separation of the 
two formations in the Stonewall quadrangle. Because of a desire 
to prevent confusion which might arise by abandoning either of 
these well established names, however, the attempt has been 
made. The Savanna-Boggy contact as drawn, therefore, represents 
what is thought to be the most probable conditions, nevertheless, 
only approximate. 


76 


SAVANNA FORMATION 


Fauna of the Savanna formation 


SPECIES 

15 

LOC 

22 

ALIT 

44 

IES 

45 

47 

ANTHOZOA 







C 











ECHINOIDEA 







R 





BRYOZOA 






Acanthoclema csrfaonfif'iiim n. sp 

R 






c 











BRACHIOPODA 






Ohnnptps granulifp.r . . 

C 




A 

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R 


C 



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R 





Dprhya r.rassa . 

R 




R 

IVTarginifpra miirir.at.a 

A 





Productus cora . . __ 



c 


CF 

Pnstnla nehraskensis . 



R 



Spirifpr r.ameratns ... 

A 





Spirifer rockymontanus . . 



R 


R 

PELECYPODA 






Aeanthopecten carboniferus . ... 

A 


R 



Allorisma terminal e.. 




R 


Astartella concentrica... 





R 

Aviculopinna americana . . ... . 



R 



Leda bellistriata .... .. .. 

R 


R 


A 

Myalina swallovi . 



C 



Schizodus sp______ 


R 




GASTEROPODA 






Bellerophon bellus....... 


CF 




Bellerophon crassus wewokanus..... 

R 

c 




Bucanopsis meekiana______ 


C 




Euphemus carbonarius..... 

A 

C 




Murchisonia terebra......... 


? 



R 

Phanerotrema grayvillense....... 





C 

Pleurotomaria monilifera..... 




R 


Worthenia tabulata... 

R 





CEPHALOPODA 






Coloceras liratum....... 




CF 

R 

Coloceras sp 


R 





A—abundant. C—common. R—rare. 


















































































BOGGY FORMATION 


77 


FOSSILS 

See accompanying chart. 

AGE AND CORRELATION 

The Savanna formation is equivalent to the lower part of the 
Mineral Wells formation of Texas, and to the greater part of the 
Cherokee of Kansas ancj Missouri. 

STRUCTURE 

The normal dip of the Savanna strata is toward the north and 
northeast. South of Jesse are a number of prominent sand¬ 
stone beds that are highly tilted and which give some indications of 
a northwest-southeast fault. The weight of evidence, however, is 
in favor of only sharp folding rather than faulting. In the north¬ 
east corner of section 11 the sandstones mentioned show dips both 
to the northeast and southwest of a narrow anticlinal axis. Far¬ 
ther southeast in section 12 the southwestward or reversal dips 
were not observed so that the narrow fold evidently opens rapidly 
in that direction. The series of sandstones when traced to the east 
side of section 12 are found to make a sharp right-angle turn to¬ 
ward the north and with a west dip continue in this direction for al¬ 
most half a mile when the strike again turns toward the east. 

ECONOMIC IMPORTANCE 

In the Coalgate folio the Savanna formation is indicated as 
containing sandstones suitable for building. In the Stonewall quad¬ 
rangle, however, no beds were observed which were thought to be 
especially suitable for such a purpose. 

BOGGY FORMATION 

NAME 

The Boggy formation was first described in 1899. 59 The de¬ 
rivation of the name is not known, but is probably from one or all 
of the several creeks of this name which cross the outcrop of the 
formation in the Coalgate quadrangle. No type section is given. 

AREAL DISTRIBUTION 

In the Stonewall quadrangle the main outcrop of the Boggy 
formation occurs as two westward pointing wedges, the reentrant 
between the two being represented by the much older formations 
that outcrop on the Lawrence uplift. The total areal extent is ap¬ 
proximately 65 square miles. 

THICKNESS AND CHARACTER 

The formation consists of sandstones, shales, and a few lime¬ 
stones. Of the three kinds of strata the shales constitute by far 


39 Taff, J. A., U. S. Geol. Survey 19th Ann. Rept. Part 3, p. 438. 



78 


BOGGY FORMATION 


the greatest thickness, but at the top of the formation clastic beds 
are quite prominent. These grade from sandstones and fine grained 
conglomerates at the eastern edge of the area to coarse limestone 
conglomerates near the town of Franks. In the latter area Boggy 
strata constitute a large part of what has previously been called the 
Franks conglomerate. 

Fifteen feet below the top of the formation, and exposed only 
in the eastern part of T. 3 N., R. 7 E., is a limestone which 
carries great numbers of the species Campophyllum torquium. The 
bed is important in that it represents the only horizon in the entire 
area where the genus Campophyllum was found and for this reason 
sTongly suggests the correlation of this member with the Cup Coral 
member of the Glenn formation south of the Arbuckle Mountains. 
About one mile east of the town of Mill Creek, in the Tishomingo 
folio, is a cup coral zone exposed near the top of the Penn¬ 
sylvanian section there. This also may be equivalent to the lime¬ 
stone near the top of the Boggy. 

The maximum thickness of the formation along the border 
of the Stonewall and Coalgate quadrangle amounts to less than 
1,300 feet. If the upper part of the formation were present in the 
region south of Stonewall, however, it is probable that the thick¬ 
ness there would amount to as much as 1,500 feet. Taff’s thickness 
of 2,000 to 2,600 feet is erroneous for the western part of the 
Coalgate quadrangle. The large thickness given by him being due 
apparently to the fact that he did not recognize the fault north of 
Stonewall which causes a repetition of almost the entire Boggy 
section. 

In the vicinity of Franks only the upper part of the formation 
is exposed, but it is thought that wells drilled there would encounter 
a full section of possibly 1,500 feet. On the eastern end of the 
Lawrence uplift the lower part of the Boggy is in unconformable 
contact with the Caney shale and the Wapanucka limestone. On 
the northern flank of the uplift, near Lawrence, it overlaps all lower 
formations from Caney to Viola, inclusive. 

Because of the pronounced fault that separates the Franks gra- 
ben from the Lawrence uplift, lower Boggy strata on the north are 
in contact with upper Boggy beds to the south of this fault. From 
the point at which the fault cuts it off, the lower contact of the 
formation extends northwestward across the Lawrence uplift, and in 
the north central part of sec. 15, T. 3 N., R. 6 E., terminates against 
another fault which marks the north side of the Lawrence uplift 
(horst). At the latter point the lower Boggy is in contact with 
upper Wewoka strata; the intervening Thurman, Stuart, Senora, Cal¬ 
vin, Wetumka, and lower Wewoka formations being fauTed down to 
the north. One-half mile farther west is an outlier of Boggy to 


CROSS SECTION THROUGH SECS. 3 AND 10, T 3 N., R. 7£. 


STRATIGRAPHY 


79 



u 

s~ 

3 

bC 

IZ 


























80 


BOGGY FORMATION 


the south of this fault. Here then is represented only about 200 
feet of the lower part of the formation. The outcrop of the out¬ 
lying portion appears as a narrow band extending along a south¬ 
eastward facing escarpment. It is capped by a thin section of over¬ 
lapping beds belonging to the upper part of the Wewoka formation. 
North of Lawrence the Boggy passes beneath the Seminole forma¬ 
tion which overlaps onto the Viola limestone. As is the case with 
all the formations above the upper part of the Atoka, certain strata 
of the Boggy carry small amounts of chert fragments. Taflf 60 men¬ 
tions chert conglomerates as being common in the formations of the 
Coalgate quadrangle and suggests as a source of the material the 
Talihina (Ordovician) chert which outcrops in the Ouachita area 
southeast of Coalgate. This suggestion receives support from ob¬ 
servations made in the present survey and will be mentioned again 
in the discussion of later formations. The evidence contributed by 
well logs indicates that, throughout all the area of the Stonewall 
quadrangle, north of the Lawrence uplift, the Boggy rests directly 
upon the Wapanucka and Caney formations. 

FOSSILS 

The Boggy formation has a very rich fauna. The shales es¬ 
pecially carry numerous and well preserved specimens. The fossils 
identified from the Boggy are listed on the accompanying chart. 

AGE AND CORRELATION 

The Boggy formation is here correlated with most of the upper 
portion of the Mineral Wells formation of Texas, and with the lower 
part of the Marmaton and the upper part of the Cherokee of Kan¬ 
sas and Missouri. 


STRUCTURE 

As has been stated, the main outcrop of the Boggy formation 
in the Stonewall quadrangle consists of two westward-pointing 
wedges. The southernmost of these is broadly anticlinal. The 
flanks of the fold being marked by sharp synclines. The anticline 
opens broadly toward the east and plunges westward into the 
Franks graben. The syncline along the northern edge of this out¬ 
crop is the result of fault drag as is also the case with the western 
portion of the syncline that extends along the southern edge of the 
outcrop. 

The normal dip of that portion of the formation which is ex¬ 
posed on the eastern end of the Lawrence uplift is toward the north¬ 
east. The dip of the narrow outcrop north and northeast of Law¬ 
rence is toward the northwest. 


60 U. S. Geo. Survey, 19th Ann. Rept. Pt. 3, p. 442, 1899. 



BOGGY FORMATION 


81 


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Fauna of the Boggy formation—Continued 


82 


BOGGY FORMATION 


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Fauna of the Boggy formation—Continued 


BOGGY FORMATION 


83 


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PELECYPODA....Continued 

Yoldia glabra. 

TRILOBITA 

Griffith ides parvulus_ 

GASTROPODA 

Bellerophon crassus wewokanns 

Bellerophon marcouanus 

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84 


THURMAN SANDSTONE 


ECONOMIC IMPORTANCE 

The Boggy formation is the source of the shallow oil in the 
Allen field, the 1,300-foot gas in the Ada field, and possibly the 
shallow oil at Beebe. 


THURMAN SANDSTONE 

NAME 

The name and first description of the formation is by Taff. 61 
He does not explain the derivation of the term, but it is probably 
after the town of Thurman located in the Canadian quadrangle. 
No type section was given. 

AREAL DISTRIBUTION 

The outcrop of Thurman sandstone in the Stonewall quad¬ 
rangle is very small. An outlier representing the basal part of the 
formation caps the southward-facing escarpment which extends 
along the line between secs. 7 and 18, T. 3 N., R. 8 E. From the 
northern part of sec. 7, T. 3 N., R. 8 E., the main outcrop extends 
southward to the northeastern part of sec. 16, T. 3 N., R. 7 E., 
and is there cut off by a fault. In the western part of this section 
the Thurman reappears on the north side of the fault and extends 
westward into sec. 18 where it terminates against what is thought 
to be an extension of the same fault that passes through section 16. 

It is possible that Thurman strata are also present in the Franks 
graben. If so, such beds are confined to a small area along the north 
side of the graben and just south of the eastern end of the outcrop 
of Hunton formations on Bois d’Arc Creek. In the absence of 
proof that the formation is represented there the entire area has 
been mapped as Boggy. 

THICKNESS AND CHARACTER 

A complete section of the Thurman formation in the Stone¬ 
wall quadrangle is about 100 feet. Several beds of conglomerate 
and conglomeratic limestones occur in the basal part of the section. 
The pebbles in these beds are waterworn and consist of chert and 
limestone. Some of the limestone fragments greatly resemble the 
pink crinoidal member of the Chimneyhill limestone and are 
thought to have been derived from that formation. 

Brown and yellowish-brown sandstones are very prominent 
in the formation and alternate with dark colored shales. 

Fifteen feet below the base of the formation occurs the very 
characteristic Campophyllum-bearing limestone mentioned in the 
discussion of the Boggy formation. 


€1 Taff, J. A., U. S. Geol. Survey 19th Ann. Rept. Pt. 3, p. 439, 1899. 



STUART SHALE 


86 


This bed is easily traceable and clearly defines the base of the 
Thurman. The top of the formation, however, is not so easily de¬ 
termined. In the Coalgate folio the upper limit coincides with the 
outcrop or a rather heavy sandstone, and although there are other 
sandstone beds above this one, it was taken as the top of the for¬ 
mation and mapped westward into the Stonewall quadrangle as the 
upper limit of the Thurman. 

FOSSILS 

Only one collection was made from the Thurman. This was 
from a conglomeratic limestone near the base of the formation and 
contained the following fossils: 

Allorisma sp., Euphemus nodocarinatus, Hustedia mormoni, Par- 
alledon sp., Productus cora and Schizodus affinis. 

AGE AND CORRELATION 

The Thurman sandstone is here correlated with the upper part 
of the Mineral Wells formation of Texas, and with the middle por¬ 
tion of the Marmaton of Kansas and Missouri. 

STRUCTURE 

The Thurman sandstone marks a change in the normal strike 
of the formations which outcrop in the eastern part of the Stonewall 
quadrangle. The normal dip of all the older strata in this part of 
the area is toward the northeast, but in the case of the Thurman it 
is north and slightly west of north. The structure of the Thurman 
and the upper part of the underlying Boggy formation is quite com¬ 
plicated and is discussed more in detail in the chapter on structure. 

STUART SHALE 

NAME 

The Stuart shale presumably received its name from the town 
of Stuart which is located on the outcrop of the formation in the 
Coalgate quadrangle. The formation was first described by Taff. 62 

AREAL DISTRIBUTION 

In the Stonewall quadrangle the Stuart shale outcrops along a 
very prominent southward facing escarpment. It enters the area 
through the southern part of section 6 and the northern part of sec. 
7, T. 3 N., R. 8 E., and may be traced in a general southwestward 
direction to the north central part of sec. 17, T. 3 N., R. 7 E. From 
here westward the outcrop is concealed in the valley of Clear Boggy 
Creek. It is assumed that the formation terminates westward in 
the angle formed by the two faults which intersect in the western 
part of sec. 18, T. 3 N., R. 7 E. 


62 Taff, J. A., U. S. Geol. Survey Geol. Atlas, Coalgate Folio No. 74, 1901. 



86 


SENORA FORMATION 


The average width of the formation is less than one-fourth 
mile. In the southern part of section 9 and the northern part of 
sec. 16, T. 3 N., R. 7 H., the outcrop is quite narrow. The topo¬ 
graphic relief here is not unusual and as the dip of the formation 
does not seem sufficient to account for the full section it is thought 
that the strata are cut by a fault of small throw. 

THICKNESS AND CHARACTER 

The thickness of the Stuart shale is approximately 80 feet. It 
consists of dark shales ranging through shades of green, blue, and 
black, and near its top and bottom also carries a few thin beds of 
sandstone. About 15 feet below the top- of the formation is 
generally a zone of brown concretions, which were of assistance in 
mapping. 


FOSSILS 

No collections were made from the Stuart shale, although sev¬ 
eral beds were observed to be slightly fossiliferous. From a fine¬ 
grained limey sandstone just above the formation, in the base of 
the overlying Senora formation, the following species were collect¬ 
ed at locality 159. 

Allorisma costatum, Astartella concentrica, Aviculopinna 
americana, Aviculopecten occidentalis, Chonetes mesolobus. Leda 
bellistriata, MeekospLa peracuta, Productus cora, and Myali.na 
swallovi. 


AGE AND CORRELATION 

The Stuart shale is thought to be equivalent to the basal por¬ 
tion of the Palo Pinto formation of Texas, and a portion of the up¬ 
per Marmaton of Kansas and Missouri. 

STRUCTURE 

The normal dip of the formation is between three and four 
degrees in a direction slightly west of north. 

SENORA FORMATION 

NAME 

The name of the formation is by Taff. 63 The term was prob¬ 
ably derived from the old post village of that name which was lo¬ 
cated in what is now the southern part of Okmulgee County. The 
village does not appear on recent maps. 

AREAL DISTRIBUTION 

At the eastern edge of the quadrangle the Senora outcrop has 


63 Taff, J. A., U. S. Geol. Suivey, Atlas, Coalgate folio, No. 74, 1901. 



SENORA FORMATION 


a width of about one and one-half miles. Because of faulting and 
more intense folding the exposure narrows toward the southwest. 
Near the western edge of T. 3 N., R. 7 E., the outcrop enters the 
valley of Clear Boggy Creek and can not there be identified. It is 
thought that the Senora formation is cut off toward the west by the 
northeast-southwest fault that passes through the northern part of 
sec. 18, T. 3 N., R. 7 E. 

THICKNESS AND CHARACTER 

In a section measured through the central part of secs. 3 and 
10, T. 3 N., R. 7 E., the Senora was found to be 125 feet thick. At 
the base of the formation there is about 35 feet of sandstone with 
only a few thin beds of interstratifled shale. This series of beds is 
much more resistant than the underlying Stuart shale and the dif¬ 
ferential weathering of the two results in the formation of a steep, 
southward facing escarpment. The Stuart shale occupies the steep 
face of the escarpment and the basal Senora beds extend along the 
crest. (See cross section, figure 1, page 79). 

Above the basal sandstone, to the top of the formation, shales 
are prominent, but interbedded with these are brown and yellowish- 
brown sandstones. 

In the basal sandstones there is locally a thin, arenaceous 
limestone that is quite fossiliferous. This bed is of assistance in 
mapping as is also the zone of concretions fifteen feet below the 
base of the formation. 

The contact between the Senora formation and the Calvin 
sandstone as here mapped is only approximate. About 125 feet 
above the base of the Senora and near the base of the shale (We- 
tumka), that occurs below the Wewoka formation, is a series 
of sandstones that weather out as a low, rounded ridge. These strata 
were taken to represent the Calvin sandstone. The upper limit of 
the Senora was drawn along their basal contact. 

FOSSILS 

A rather large fauna was collected from the Senora and is 
listed on the accompanying chart. Probably the most characteristic 
fossil of the formation is Conularia crustnla which occurs in great 
abundance near the base. 

AGE AND CORRELATION 

The Senora formation is correlated with the middle portion of 
the Palo Pinto formation of Texas, and is equivalent to a part of the 
upper Marmaton of Kansas and Missouri. 

STRUCTURE 

The normal dip of the formation is toward the northwest. 


88 


SENORA FORMATION 


Fauna of the Senora formation 


SPECIES 

LO( 

158 

:alti 

159 

"TES 

163 

BRACI1IOPODA 




Ambocoelia planoconvexa ___ 



A 

Chonetes mesolobus ... 


C 


Derbya crassa . .-.- 



R 

Marginifera muricata ... 



A 

Productus cora .... 


G 

A 

Pugnax rockymontanus .. 

R 


C. 





Roemerella patula . ___ 

R 


R 

PELECYPODA 




Allorisma sp.......... 



R 

Allorisma costatum . ... 


R 


Anthroconeilo taffiana... ... 



C 

Astartella concentrica........ 


R 

C 

Astartella varica____ 



C 

Aviculopecten occidentalis. ... 


R 


Aviculopinna americana________ 


A 

R 

Deltopecten texanus .... . 

K 



Edmondia? reflexa . .... . 



R 

Leda bellistriata. . ..... 


R 

R 

Led a bellistriata attenuata______ _ 

R 


C 

Myalina swallovi_________ 


R 


Nuculopsissp. . . .... ... 



('. 

Nuculopsis ventricosa......... 

R 


c 

Pleurophorous cf. subcostatus..... 



R 

Schizodus alpinus......... . 



R 

Yoldia glabra ... . 



C 

GASTROPODA 




Bellerophon marcouanus.. 



R 

Meekospira peracuta choctawensis .. 


R 

c 

Phanerotrema grayvillense........... 

9 



Pleurotomaria perhumerosa......... 



R 

Sphaerodoma brevis ................. 



R 

Trepospira depressa........ 



C 

Worthenia tubulata. . ..... 



A 

PTEROPODA 




Coi ularia crustula..... 

A 


R 

CEPHALOPODA 




Coloceras liratum... 

R 


R 

Gastrioceras sp. 



T~> 


A—abundant. C—common. R—rare*. 
































































CALVIN SANDSTONE 


89 


Toward the eastern edge of the quadrangle the strike swings slightly 
more toward the northeast than is the case with the underlying 
Stuart and Thurman formations. 

CALVIN SANDSTONE 

NAME 

The Calvin sandstone was named and first described by Taff. 64 
He does not give a type area for the formation, but it seems prob¬ 
able that the name is after the town of Calvin, located in the north¬ 
ern part of the Coalgate quadrangle. 

AREAL DISTRIBUTION 

On the maps of the Coalgate folio the outcrop of the Calvin 
sandstone, at the western edge of the quadrangle, is shown to have 
a width of two miles. Continuing southwestward into the Stone¬ 
wall quadrangle, and on strike with this outcrop, there are a number 
of sandstone ledges. These strata with their interbedded shales 
constitute the Calvin formation and can be traced for a distance of 
about two miles. After this the upper, and then successively lower 
beds, either pinch-out or grade into shales. 

On the areal map of the Stonewall quadrangle the upper limit 
of the Calvin is drawn at the top of the continuing sandstones. For 
this reason the thickness and width of the outcrop diminishes very 
rapidly toward the southwest. If the upper sandstones of the Coal¬ 
gate exposure disappear by gradation into shales rather than by 
thinning, it is probable that beds here mapped as lower Wetumka 
are, in reality, upper Calvin. This possibility is somewhat indicated 
by the fact that the Wetumka shale, as mapped, has a thickness of 
250 feet while in the Coalgate area it averages only 120 feet. 

In the absence of evidence to clearly establish the gradation 
of sandstones into shales the upper limit of the mappable sand¬ 
stones was taken as the top of the Calvin formation, and the forma¬ 
tion is assumed to thin rapidly toward the southwest. 

Toward the southwest the formation could not be traced be¬ 
yond the western side of sec. 9, T. 3 N., R. 7 E. It is probable that 
the formation is there cut off by an eastward extension of the fault 
that passes through the northern part of section 18, of the same 
township and range. 

THICKNESS AND CHARACTER 

A section measured in the central part of sec. 3, T. 3 N., R. 
7 E., near the western end of the outcrop shows a thickness of only 
40 feet for the Calvin. 


64 Taff, J. A., U. S. Geol Survey, Geol. Atlas, Coalgate Folio, No. 74, 1901. 



90 


CALVIN SANDSTONE 


Where this section was taken the beds assigned to the Calvin 
consist of coarse-grained, brown and grayish-brown sandstones. With 
these are interbedded a few thin layers of shale. The beds are 
slightly more resistant than the shales of the upper Senora and 
lower Wetumka, and for that reason weather out as low, rounded 
ridge. 

PLATE XI 



THIN-BEDDED CALVIN SANDSTONE IN NORTHEAST CORNER 
SEC. 36, T. 4 N., R. 7 E. 


Farther northeast, and typically in the northeast corner of 
sec. 36, T. 4 N., R. 7 E., some of the sandstones are very thin bed¬ 
ded. (Plate XI) Associated with these are occasional red shales. Such 
a red shale occurs in the road one-half mile south of the corner 
just mentioned. 


FOSSILS. 

No fossils were found in the Calvin sandstone. 

AGE AND CORRELATION. 

On the basis of the fauna contained in associated beds the 
Calvin is correlated with an upper portion of the Palo Pinto forma¬ 
tion of Texas, and with a zone near the top of the Marmaton of 
Kansas and Missouri. 



WETUMKA SHALE 


91 


WETUMKA SHALE 

NAME 

The Wetumka shale was named by Taff. 65 He does not de¬ 
scribe a type section, but it is probable that the name of the forma¬ 
tion was taken from the town of Wetumka which is located in 
the Wewoka quadrangle. 

AREAL DISTRIBUTION 

In the Stonewall quadrangle the outcrop of the Wetumka 
shale has an average width of less than a mile. It enters the area 
near the west central part of T. 4 N., R. 8 E., and extends in a south¬ 
westerly direction to a point a short distance west of Clear Boggy 
Creek. 

In the western part of sec. 18, T. 3 N., R. 7 E and the eastern 
part of sec. 13, T. 3 N., R. 6 E., it is cut off by a fault. 

THICKNESS AND CHARACTER 

In sec. 24, T. 4 N., R. 7 E., the Wetumka shale has a thickness 
of between 150 and 175 feet, while a section measured in sec. 3, 
T. 3 N., R. 7 E., shows a total of 250 feet. As pointed out in the 
discussion of the Calvin formation this apparent difference in thick¬ 
ness is probably due to the fact that in section 3, some of the upper 
shaly strata of the Calvin have been mapped as basal Wetumka. 
The contact between the two formations is gradational and, at least 
in the Stonewall quadrangle, it would probably be more advisable 
to map the formations together. They extend only a short distance 
into the area, however, and in an endeavor to preserve the strata- 
graphic subdivisions used in the Coalgate folio a separation of the 
formations has been attempted. 

There are a few thin sandstones near the top and bottom, but 
for the most part the formation consists of almost unbroken shale. 

The slight resistance offered to erosion by this shale results 
in its being undercut from beneath the resistant sandstones in the 
base of the overlying Wewoka formation, and in the formation of 
a prominent southeastward-facing escarpment. 

FOSSILS 

The top of the Wetumka is especially fossiliferous. Some 35 
species were collected from the formation and are listed in the 
accompanying chart. 

AGE AND CORRELATION 

In computing the percentage of species common to the Penn¬ 
sylvanian strata of the Stonewall quadrangle and to the Pennsyl¬ 
vanian of surrounding areas it appears that the Wetumka shale is to 

65 Taff, J .A., U. S. Geol. Survey, Geol. Atlas, Coalgate Folio No. 74, 1901. 


92 


WETUMKA SHALE 


Fauna of the Wetumka formation 


SPECIES 


ANTHOZOA 


Lophophyllum profundum. 


BRYOZOA 


Fenestella sp. 


BRACHIOPODA 


Ambocoelia planoconxexa. 

Derbya crassa. 

Lingula umbonata.. 

Marginifera muricata.. 

Marginifera splendens._.. 

Productus cora.. 

Pugnax rockymontanus. 

Roermerella patula. 


PELECYPODA 


Allorisma terminale..._. 

Anthroconeilo tafiiana_ 

Astartella concentrica._. 

Astartella varica. 

Aviculopinna americana. 

Edmondia? reflexa._. 

Leda bellistriata... 

Leda bellistriata attenuata.—. 

Nucula anondontoides. 

Nuculopsis ventricosa. 

Nuculopsis sp. 

Pleurophorus cf. subcostatus. 

Schizodus alpinus.. 

Schizodus sp. 

Yoldia glabra.. 


GASTROPODA 


Bellerophon marcouanus.. 

Meekospira peracuta choctawensis. 

Pleurotomaria perhumerosa.. 

Sphaerodoma brevis.. 

Trepospira depressa... 

Worthenia tabulata..._.. 


PTEROPODA 


Conularia crustula- 


CEPHALOPODA 


Coloceras liratum. 

Gastrioceras sp.. 

Orthoceras tuba. 


LOCALITIES 


163 


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C—common. R—rare. 












































































WEWOKA FORMATION 


93 


be correlated with the upper part of the Palo Pinto formation and 
the lower part of the Garford formation of Texas, and with the up¬ 
per portion of the Marmaton of Kansas and Missouri. 

STRUCTURE 

The strike of the Wetumka shale shows a continued swing 
toward the northeast. The gradual change in strike of progressively 
higher beds from northwest-southeast, as in the case of the Boggy 
formation, to northeast-southwest in the case of the Wetumka may 
be appreciated better by referring to the areal map. 

WEWOKA FORMATION 

NAME 

The name of this formation is from the town of Wewoka in 
the Wewoka quadrangle. Taff 66 is the nomenclator, and is the one 
who defined and first described the formation. 

AREAL DISTRIBUTION 

In the Stonewall quadrangle the Wewoka formation has an 
areal extent of approximately 3 5 square miles. Throughout T. 
4 N., R. 7 E., the average width of the outcrop is nearly three miles, 
but in the northern part of T. 3 N., R. 6 E., the basal, and then (west¬ 
ward) successively higher and higher beds are cut off by the east- 
west fault that marks the northern side of the Lawerence uplift. 
For this reason the outcrop along the fault narrows westward very 
rapidly. At a point just west of the main road, about two miles 
south of Ada, the upper 30 or 40 feet of the formation extend south¬ 
ward across the fault and rest unconformably upon the Boggy for¬ 
mation. Although sharply folded along the fault zone this upper 
portion of the formation is not broken and appears to have been 
deposited after the main period or periods of faulting. 

From the point at which the upper beds cross the fault they 
may be traced as a narrow band near the top of the steep, south¬ 
eastward-facing escarpment that extends from the northeastern 
part of sec. 16, T. 3 N., R. 6 E., to the vicinity of Lawrence. Near 
the southwestern corner of sec 19, T. 3 N., R. 6 E., the upper beds 
of the Wewoka formation appear to pinch-out with the result that 
the next higher, Holdenville, formation rests directly upon the 
Boggy. 

The Wewoka formation is also thought to be present in the 
Franks graben. Extending north and south through the central 
part of T. 2 N., R. 6 E., and typically exposed in the section line nt 
the extreme northeast corner of section 23, is a heavy sand¬ 
stone that in lithologic appearance greatly resembles the upper 


66 Taff, . T . A., U. S. Geol. Survey Geol. Atlas, Coalgate Folio No. 74, 1901. 



96 


WE WOK A FORMATION 


Allen and beyond the limits of the Stonewall quadrangle, there is 
a conglomerate 67 that is very unusual. It differs from the sedi¬ 
ments below the Pontotoc terrane in that it carries pebbles of 

PLATE XIII 



SANDSTONE MEMBER AT THE TOP OF THE WEWOKA FORMATION. 
Top of eastward-facing escarpment, in the northeast quarter of sec. 16, T. 3 
N., R. 6 E. Below this member is about 15 feet of Wewoka shale 
which rests unconformably on the Boggy formation. 

igneous material. The bed could be traced for only a few hundred 
yards. The igneous material contained is darker and more fine- 

67 For a further discussion of this deposit see Circular 11, Paper No. 2 of the 
Okla. Geol. Survey. 








Fauna of the Wewoka formation 


WEWOKA FORMATION 


97 



♦Found by Girty in the Wewoka formation outside of the Stonewall quadrangle. 










































































































94 


WEWOKA FORMATION 


sandstone ledge of the Wewoka. The identification of typical 
Holdenville fossils in the shales above this formation lends strength 
to the conclusion that this sandstone represents the upper member of 
the Wewoka. Beneath the sandstone at this place there are about 
125 feet of shales, limestone conglomerates, and thin limestones, 
which resemble the upper Wewoka in its development just north¬ 
ward and to the south of the fault in the northern part of T. 3 N., 
R. 6 E. 

THICKNESS AND CHARACTER 

Several sections measured in the Stonewall quadrangle show 
a total average thickness of 400 feet for the Wewoka. The top 
and bottom of the formation are marked by definite sandstone 
ledges that were mapped without difficulty. The basal sandstone, 
as well as several other members, locally grades into chert con¬ 
glomerate. The most extensive development of such conglomer¬ 
ate in the basal member of the formation occurs at the top of the 
escarpment in the northern part of sec. 18, T. 3 N., R. 7 E. A little 
over a mile northeastward a thick chert conglomerate also caps 
the high point that projects southward from section 4, into the 
northern part of section 9. This deposit represents a local develop¬ 
ment in what is normally a sandstone that occurs about 90 feet 
above the bottom of the formation . Many other sandstones in the 
formation also carry small quantities of chert conglomerate, tut by 
far the greatest development of this type of clastic material is in the 
two members that occur at the base and approximately 90 feet 
above the base of the formation, respectively. 

In the upper part of the formation there are several very 
characteristic beds among which there is a thin limestone that is 
rich in specimens of Fusulina. Near the center of the formation in 
sec. 5 T. 4 N., R. 8 E., several cross-bedded sandstones were ob¬ 
served. 

The top of the sandstone bed, which marks the top of the 
formation, locally grades into limestone. This development is 
quite common from the southwestern part of T. 4 N., R. 7 E., north¬ 
eastward to the edge of the quadrangle. In the vicinity of the fault 
in the northern part of T. 3 N., R. 6 E., no lime was observed at the 
top of this bed, but southward, beyond the fault, it again appears. A 
limestone also occurs at the top of the sandstone which is thought 
to represent the top of the Wewoka in the Franks graben. 

In the northern part of T. 3 N., R. 6 E., limestone conglomer¬ 
ates are quite common in the upper part of the Wewoka formation. 
That these conglomerates were derived from the Arbuckle Moun¬ 
tains is indicated by the contained fragments, many of which close¬ 
ly resemble the Hunton and Viola limestones. (Plate XII A.) 

Just east of the center of sec. 32, T. 5 N., R. 8 E., southwest of 


PLATE XII 



A. LIMESTONE CONGLOMERATE IN THE WEWOKA FORMATION, IN 
THE SOUTHEAST CORNER SEC. 11, T. 3 N„ R. 6 E. 



B, CROSS-BEDDED SANDSTONE IN THE WEWOKA FORMATION, 

IN SEC. 5, T. 4 N., R. 8 E. 









Fauna oj the Wewoka formation—Continued 


98 


WEWOKA FORMATION 


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Fauna of the Wewoka formation—Continued 


WEWOKA FORMATION 


99 




Found by Girty in the Wewoka formation outside of the Stonewail quadrangle. 

























































































100 


WEWOKA FORMATION 


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HOLDENVILLE FORMATION 


101 


grained than the average arkosic material which is so common in 
the Pontotoc beds and it seems improbable that the two were de¬ 
rived from the same source. The nature of the igneous material in 
the Pontotoc strata and the fossiliferous limestone fragments asso¬ 
ciated with it clearly indicates that it was derived from the Arbuckle 
Mountains. The source of the igneous pebbles in the Wewoka 
occurrence, however, is unknown. The pebbles are mostly small 
and well rounded and may have been brought in from a distant 
region. 


FOSSILS 

The Wewoka’formation has a very prolific fauna that has been 
described and figured by Girty 68 . 

Species collected from the formation in the course of the pre¬ 
sent investigation as well as the species that were found by Girty 
and not collected by the writer are listed on the accompanying 
chart. 


AGE AND CORRELATION 

The Wewoka formation is correlated with the upper Graford, 
the Brad, and the Caddo Creek formations of Texas, and with the 
Kansas City formation of Kansas and Missouri. 

STRUCTURE 

Throughout most of its length the Wewoka outcrop has a 
normal northwestward dip that closely conforms to that of the 
underlying Wetumka shale. In the northern part of T. 3 N., R. 6 E., 
however, the dip has been controlled by the east-west fault that pas- 
es through that area. In this region the dip is high and is almost 
directly toward the north. The thin section of Wewoka that occurs 
to the South of the fault just mentioned dips at a low angle 
toward the northwest. It here rests unconformably on the beveled 
edges of highly folded Boggy strata. 

HOLDENVILLE FORMATION 

NAME 

The formation takes its name from the town of Holdenville 
in the Wewoka quadrangle. It was named and first described by 
Taff 69 . 

AREAL DISTRIBUTION 

In the Stonewall quadrangle the outcrop of the Holdenville 
formation varies in width from more than two miles, in the vicinity 

68 Girty, Geo. H., U. S. Geol. Survey, Bull. 544, 191 5. 

69 Taff, J. A., U. S. Geol. Survey, Geol. Atlas Coalgate Folio No. 74, 1901. 



102 


HOLDENVILLE FORMATION 


of Canadian River, to less than one-fourth mile as at several points 
south and southwest of Ada. The formation extends from the 
northeast corner of the area southwestward to the eastern part of 
sec. 23, T. 3 N., R. 5 E., At the latter point it is overlapped by the 
Seminole formation. The town of Sasakwa is located on the upper 
part of the formation while Francis, Oakman, and Ada each lie 
about a mile to the west of the upper limit of the outcrop. 

Because of folding, faulting, and subsequent erosion no strata 
of the Franks graben, that occur higher than the lower part of the 
Boggy formation, can be traced beyond the limits of that area. 
Faunal and lithologic similarity, between strata within the graben 
and beds near the top of the Wewoka formation to the north of the 
Lawrence uplift, leads to the conclusion that the Wewoka is present 
in the graben 70 . On similar, but more conclusive evidence it is also 
established that the Holdenville formation is represented there. 

Above the thick sandstone, that is thought to be the top bed 
of the Wewoka, there is, in the graben, a series of shales, sandstones, 
and limestone conglomerates that carry a fauna which resembles 
that of the Holdenville formation. At the old asphalt pit in the 
southern part of sec. 20, T. 2 N., R. 6 E., (Locality 79) there is 
an asphaltic conglomerate with a rich fauna. This fauna so closely 
resembles the Holdenville collection that there can be but little 
doubt that its containing strata are a part of that formation. 

Further evidence that Holdenville strata occupy a part of the 
Franks area is afforded by the shale which is exposed in the south¬ 
western part of sec. 15, T. 2 N., R. 6 E. This shale carries a fauna 
the general assemblage of which indicates its correlation with the 
thick shale near the base of the Francis formation. Below the shale 
is a limestone that probably represents the southward exten¬ 
sion of the DeNay limestone member. From the probability of 
normal stratigraphic position the interval between the top of the 
Wewoka formation and the base of the supposed DeNay limestone 
represents the Holdenville and Seminole formations. 

In the Franks area evidence was not secured which would 
justify the establishment of a contact between the Holdenville and 
the supposedly overlying Seminole. This lack of evidence is indi¬ 
cated on the areal map by a gradation of the symbols representing 
the two formations. 


’° See discussion of the Wewoka formation. 



HOLDENVILLE FORMATION 


103 


THICKNESS AND CHARACTER 

The Holdenville formation consists largely of shale, but also 
contains numerous sandstone beds and two mappable limestone 
members. Some of the sandstones locally develop into massive 
chert conglomerates that are lithologically identical with the con¬ 
glomerate at the base of the Seminole in the type area of that for¬ 
mation. 

In the northeastern part of the quadrangle the Holdenville 
is approximately 235 feet thick. It thins southward, however, and 
at its southern extremity, where it is overlapped by the Seminole, 
does not exceed 100 feet. 


PLATE XIV 



SASAKWA LIMESTONE MEMBER OF THE HOLDENVILLE FORMATION 
EXPOSED IN QUARRY ONE-FOURTH MILE SOUTH OF SASAKWA 


SASAKWA LIMESTONE MEMBER 

The upper of the two limestones occurs 35 feet below the top 
of the formation. Its outcrop passes through the town of Sasakwa 
and the member is named after that town. The bed is especially 
well exposed in the railroad cut and quarry about one-fourth mile 
south of Sasakwa. (Plate XIV). At the ford on Canadian River, be¬ 
tween Sasakwa and Francis, the member is also well exposed. 
Southwestward from the crossing on Canadian River the member 







104 


HOEDENVILLE FORMATION 


can be traced without much difficulty to the southern part of sec. 
9, T. 3 N., R. 6 E., at which place it grades into a limey shale and 
from there westward was not identified with certainty. The thick¬ 
ness of this bed is quite variable. At the northeast corner of the 
quadrangle it is about two feet; just south of Sasakwa it is at least 
15 feet, but from there southward gradually thins to a thickness of 
about one foot. The latter average thickness is maintained to the 
point at which the bed could no longer be mapped. The S'asakwa 
limestone is fossiliferous throughout, but carries its largest fauna in 
the northern part of the quadrangle. The collection from locality 
230 was taken from the railroad cut south of Sasakwa. 

HOMER LIMESTONE MEMBER 

This limestone lies below the Sasakwa limestone and is also 
best developed in the northeastern part of the quadrangle. The 
bed shows a pronounced change from north to south, but at the 
foot of the bluff in the south central part of sec. 25, T. 4 N., R. 6 E., 
the stratum shows a combination of the characteristics common to 
it, both to the north and south. This point is one-half mile west 
of Homer school and the name of the school is therefore applied 
to the bed. 

In the northeastern part of the quadrangle the Homer lime¬ 
stone is approximately three feet thick. It occurs 70 feet below 
the Sasakwa limestone and there constitutes a reef of 
Chaetetes. The color of the limestone in this area is dark gray or 
almost black. The reef-like character of the stratum is maintained 
southward to the vicinity of Homer school where the quantity of 
Chaetetes begins to diminish and a few specimens of Fusulina appear. 
In this locality the interval between the Homer and Sasakwa mem¬ 
bers has decreased to about 40 feet. In the northern part of sec. 
2, T. 3 N., R. 6 E., only a few specimens of Chaetetes are to be found 
in the bed and Fusulina is abundant. Within the space of a mile 
along the outcrop to the southwest Chaetetes entirely disappears 
and the bed becomes almost a pure Fusulina limestone. The lime¬ 
stone is never light in color, but with the advent of the great num¬ 
bers of Fusulina , toward the south, it becomes even darker than it 
is toward the north. The bed is well exposed in the little stream 
valley just south of the railroad crossing in the southern part of 
sec. 10, T. 3 N., R. 6 E. West of this point the Homer limestone 
could be traced with certainty for less than a mile. It was doubt¬ 
fully identified at several places in sec. 17, T. 3 N , 7 E. At the 
railroad crossing just mentioned the interval between the Homer 
and Sasakwa limestones is only 17 feet. 

Between these two beds, throughout all the northern portion 
of the Holdenville outcrop, there are a number of sandstones. One 


HOLDENVILLE FORMATION 


105 


or several of these quite often develops into a massive chert con¬ 
glomerate that sometimes attains a thickness of 30 feet. An ex¬ 
ample of this conglomerate occurs on the top of the hills in the 
southern part of sec. 34, T. 5 N., R. 7 E., and in the northern part 
of sec. 3, T. 4 N., R. 7 E. 

Just east of the center of sec. 8, T. 4 N., R. 7 E., at the top of 
an eastward facing bluff, there is also local development of chert 
conglomerate near the top of the Holdenville formation. 

The base of the formation is marked by the sandy limestone 
that generally occurs at the top of the upper member of the Wewo- 
ka formation. 


FOSSILS 

The fossils of the Holdenville, with those of the upper part 
of the Wewoka formation, mark a change from the faunas common 
to the lower formations. The last Chonctes mesolobus and the first 
Bnteletes hemiplicata were found in the beds of the Holdenville. 

AGE AND CORRELATION 

The Holdenville formation is thought to be equivalent to the 
Graham formation of Texas, and to the Lansing and lower Douglas 
of Kansas and Missouri. 


STRUCTURE 

In the northeastern part of the quadrangle the dip of the 
Holdenville formation averages about 160 feet per mile and is in a 
direction only a few degrees north of west. From Canadian River 
southwestward to a point east of Ada the percentage of dip re¬ 
mains the same, but the direction changes to N. 45°W. Two miles 
south of Ada, along the northern side of the fault that there marks 
the limit of the Lawrence uplift, the dip is directly north. Along 
this fault zone Holdenville beds are cut by numerous small faults, 
but the strata are generally only flexed sharplv upward toward the 
south, and in this way extended across the fault and southwestward 
to their point of overlap north of Lawrence. 

To the south of the zone of faulting the Holdenville strata 
again dip toward the northwest, while the degree of dip is much 
more gentle than it is in the region just north of the fault zone. 

In the railroad cut and quarry south of Sasakwa, the S'asakwa 
lime c tone and associated strata of the Holdenville formation are 
folded into a narrow southward plunging anticline. The south end 
of this fold is cut by a small fault which extends toward the north¬ 
east. 


Fauna of the Holdenville formation 

LOCALITIES 


106 


HOLDENVILLE FORMATION 


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Fauna of the Holdenville formation—Continued 


HOLDENVILLE FORMATION 


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108 


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SEMINOLE FORMATION 


109 


SEMINOLE FORMATION 

NAME 

The Seminole formation constitutes the youngest Pennsylva¬ 
nian sediment that occurs in that part of Oklahoma which lies to 
the east of the Stonewall quadrangle. The formation was named 
and first described by Taff, 71 and since the type area described by 
him is in the northwestern corner of the Coalgate quadrangle, near 
the edge of the Seminole Nation, it is presumed that the name 
of the formation is after that of the Nation. 

AREAL DISTRIBUTION 

The Seminole outcrop extends from the northeast corner of 
the Stonewall quadrangle southwestward to the vicinity of the town 
of Fitzhugh in the north central part of T. 3 N., R. 5 E. East and 
north of Fitzhugh the Seminole is overlapped by the Ada formation 
which normally occurs about 800 feet higher in the section. About 
one-fourth mile west of Fitzhugh a stream has cut through Ada 
strata exposing a small area of fossiliferous shales that are thought 
to belong to the Seminole. The town of Sasakwa is located on 
strata of the upper Holdenville and is just east of the eastern edge 
of the Seminole outcrop. Francis is just west of the upper or west¬ 
ern limit of the main outcrop, but upper Seminole strata are also 
exposed in the creek valley that drains into Canadian River north¬ 
westward from Francis. Oakman is about one-half mile west of 
the top of the formation, and the brick plant at the southeastern 
corner of Ada uses as a supply a shale in the base of the over- 
lying Francis formation. 

The presence of Seminole strata in the Franks graben is not 
clearly established. On the basis of evidence which indicates the 
outcrop there of the underlying Holdenville and the overlying 
Francis formation, however, it seems probable that it is there repre¬ 
sented in some part of the interval between the upper Wewoka and 
the lower Francis formations. 

THICKNESS AND CHARACTER 

Although defined by Taff the upper limit of the Seminole was 
not mapped by him. In order to establish what he considered as 
the limits of the formation his brief description and definition of 
the formation is here quoted in full. He says: 

About 50 feet of the lower part of the Seminole conglom¬ 
erate is exposed in a small area in the northwestern corner of 
the Coalgate quadrangle. This part of the formation is composed 
of laminated or stratified subangular chert, with a sprinkling of 
quartz pebbles from three inches in diameter to small grains in a cement 
of fine brown and usually ferruginous sand. The coarser conglomerate in 
the beds at the base is loosely cemented and on weathered surfaces it breaks 
down ir/to rcur.ced bowlders and loose gravel. Forty to 50 feet from the 

71 Taff, J. A., U. S. Geol. Survey, Geol. Atlas, Coalgate Folio No. 74, 1901. 



110 


SEMINOLE FORMATION 


base the conglomerate grades into brown sandstone which continues upward 
about 100 feet to the top of the formation. The Seminole formation crops 
in a rugged hilly country northwestward in the Seminole Nation, making 
rough timbe.ea lands. 

By definition then, the Seminole of the type area has a thick¬ 
ness of “about” 150 feet. Since no definite bed is named as mark¬ 
ing the top of the formation there can be no quesion as to the 
original measurement and the definition must be taken literally. 

In measuring upward and westward from the bottom of the 
50 foot chert member, (fig. 1) that occurs at the base of the 
type-section, it was found that in the extreme northeastern part of 
the Stonewall quadrangle is a thin limestone that is separated 
from the base of the Seminole by an interval which in that area 
averages 150 feet. This is a definite and persistent limestone and 
in the present work its base is taken as the top of the Seminole. 
This is the DeNay limestone. 

DeNAY LIMESTONE 

From the northeastern corner of the area, southwestward 
to a point several miles beyond Ada, this limestone has an inter¬ 
mittent outcrop that was mapped without difficulty. The bed 
was last observed in the northern part of sec. 3, T. 2 N., R. 5 E., 
almost a mile northeast of Fitzhugh. In the area to the northeast 
of Fitzhugh, where the limestone bed could not be located, the 
Seminole-Francis contact is only approximately correct. 

In sec. 5, T. 4 N., R. 7 E., this limestone is typically devel¬ 
oped on the side of an eastward facing bluff. The name of the mem¬ 
ber is after DeNay school that is located about one-fourth mile east 
of this point. 

The DeNay limestone has an average thickness of a little more 
than one foot. In the region north of Canadian River the bed is 
rather dense and breaks out in elongated blocks. In the road about 
one-half mile east of Francis the bed is slightly crinoidal. Crinoid 
stems become more abundant in the stratum toward the southwest 
and in the region south of Ada it is often almost entirely composed 
of these organisms. In the northeastern part of T. 3 N., R. 5 E., the 
crinoids become less abundant and the limestone develops a bright 
yellow color. The latter characteristic must be used with discretion 
however, because there are in the area several beds of this color. 

The basal chert that has a thickness of approximately 50 feet 
in the type area changes rapidly toward the west. In the north¬ 
eastern part of the Stonewall quadrangle its place is represented by 
several thick sandstones with interbedded shales. Locally the sand¬ 
stones carry chert conglomerates, and farther south this facies often 
becomes quite prominent. Nowhere in the quadrangle, however, was 


PLATE XV 



A. MASSIVE CHERT CONGLOMERATE, AT THE BASE OF THE SEMINOLE 

FORMATION. 

Located in the northeast quarter of sec. 18, T. 6 N., R. 8 E. This is the type 

area of the Seminole. 



B LOCAL UNCONFORMITY BETWEEN THE SEMINOLE AND HOLDEN- 

VILLE FORMATIONS. 

Location in the northeast quarter of sec. 18, T. 6 N., R. 8 E. This is the only 
locality at which an unconformity between the two formations was observed. 









112 


SEMINOLE FORMATION 


the conglomerate found to be developed to the extent that it is in 
the northwestern part of the Coalgate quadrangle. 

The basal members of the Seminole cannot everywhere be 
traced by walking. In the areas where this is the case the S'eminole- 
Holdenville contact is drawn 35 feet above the Sasakwa limestone 
member of the Holdenville formation. 

As already stated, the thickness of the Seminole formation 
in the northeastern part of the Stonewall quadrangle is, by defini¬ 
tion, about 150 feet. When the beds which limit this interval are 
traced southward, however, it is found that the interval between 
them decreases until in the region north of Fitzhugh the formation 
has a thickness Of only 90 feet. Southward from the vicinity of 
Oakman there is, about 20 feet below the top of the Seminole, a 
sandstone that is easily identifiable because of the great number 
of the species Productus insinuatus which it contains. 

FOSSILS 

Most of the shales and many of the sandstones of the Sem¬ 
inole formation are fossiliferous. The fauna collected and identi¬ 
fied is shown on the accompanying chart. 

AGE AND CORRELATION. 

The Seminole formation appears to be equivalent to the 
Harpersville and Thrifty formations of Texas, and to most of the 
Douglas of Kansas and Missouri. 

STRUCTURE 

From the northeastern corner of the quadrangle southeastward 
to the vicinity of Ada the normal dip of the Seminole formation 
averages about 100 feet per mile and is in a direction about 65 
degrees west of north. South of Ada the strike turns almost direct¬ 
ly west and continues in this direction to near the center of T. 
3 N., R. 5 E. Here it returns to a southwesterly direction which 
it maintains to its point of overlap near Fitzhugh. 

In the northern part of sec. 13, T. 3 N., R. 5 E., Seminole and 
Francis strata are cut by a small east-west fault. This fault is in 
direct alignment with the big fault in the northern part of T. 3 N., 
R. 6 E. It is believed, therefore, that below the HoldenvillB and late 
Wewoka strata the main fault, just mentioned, extends westward 
through T. 3 N., R. 5 E., and that the small fault in section 13 of 
this township represents a later movement along the already estab¬ 
lished fault plane. 


FRANCIS FORMATION 


113 


Fauna of the Seminole formation 


LOCALITIES 


SPECIES 

62 

119 

120 

128 

137 

186 

ANTHOZOA— 







Lophophvllum profundum... 




R 



BRYOZOA— 







Rhombopora lepidodendroides. 

R 



R 



BRACHIOPODA 







Aulacorhynchus millepunctatus . 

A 






Chonetes granulifer. 




A 


R 

Composita subtilita. 




A 


R 

Derbya crassa 




c 


R 

Lingula sp._ .. . 

H 






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A 

A 

R 

A 


Productus pertenuis . 

R 






Productus semireticulatus. 

? 






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R 



Spirifer cameratus 

R 



C 


C 

PELECYPODA 







Astartella concentrica 

A 






Nucula anondontoides 

It 






Pecten armigerus . . 

R 






Posodonia cf. vintonensis .. 

R 






GASTROPODA— 







Schizostoma catilloides . 

A 






CEPHALOPODA— 







Orthoceras tuba . . . 






R 

Orthoceras sp.... 

R 







A—abundant. C—common. R—rare. 


FRANCIS FORMATION 

NAME. 

This formation is here named after the town of Francis which 
is situated on the eastern edge of the outcrop. It is difficult to select 
any one section that is absolutely typical. The type area, however, 
may be considered as all that portion of the outcrop which extends 
for a distance of three miles north, and for a similar distance south, 
of Canadian River. 


AREAL DISTRIBUTION. 

In the Stonewall quadrangle the formation has an areal ex¬ 
tent of approximately 50 square miles. The outcrop extends from 
the northeastern part of the quadrangle southwestward to Fitzhugh. 























































114 


FRANCIS FORMATION 


In addition to Francis, the towns or Oakman, Hird, and the eastern 
portion of Ada are located on the outcrop. That the Francis is 
present in the Franks graben is indicated by the shale in the south¬ 
western part of sec. 15, T. 2 N., R. 6 E. The limestone concretions 
so common to the basal shale of the Francis are abundant there, 
while the lithologic character and general faunal assemblage of the 
deposit also suggests its correlation with the Francis. 

THICKNESS AND CHARACTER 

In the type area and northward the Francis formation has a 
thickness of 500 feet. In the vicinity of Ada and southward only 
the lower part of the formation is exposed, the upper part being 
overlapped by the Ada formation. 

At the base, but within the Francis formation, is the DeNay 
limestone member, the lower part of which marks the top of the 
Seminole formation. Above this limestone is an interval 
of about 30 feet that is represented by dark blue and black shales. 
These grade upward into sandstones which on the creek bluff north¬ 
west of Sasakwa have a thickness of nearly 20 feet. This is the 
sandstone that outcrops in the railroad cut below the viaduct in the 
northeastern part of Francis and is also correlated with the sand¬ 
stone ledge in the road cut just north of the brick plant and rail¬ 
road crossing near the southeast corner of Ada. Above the sand¬ 
stone member is a series of thick, dark and sometimes calca¬ 
reous shales. The average thickness of this part of the formation 
is 250 feet. In the northern part of the type area it is slightly 
more than this, but in the southern part it seems to be slightly less. 
West of Sasakwa the surface of this deposit extends to beyond the 
residence of the former Governor Brown of the Seminole Nation. 
Most of the town of Francis is located on these shales and they are 
typically developed around the water tower there. Shales of this 
member are utilized by the brick plant at Ada. As is clearly shown 
in the pit at the latter place, the lower part of the shale is much 
darker and is more calcareous than the upper part. One of the 
most characteristic features of the shale series is the abundant lime¬ 
stone concretions which it contains. These vary in size from less 
than an inch in diameter up to as much as a foot. When freshly 
broken the central mass consists of a dense, dark blue limestone, 
on weathering however, the color becomes yellow or yellowish 
brown. The concretions are often very fossiliferous. Other con¬ 
cretions collected from the shales were of the cone-in-cone type. 

Above the shale series is a thickness of almost 100 feet within 
which coarse brown sandstones and chert conglomerates predomi¬ 
nate. Only occasional fossils were found within this member. Al¬ 
though much higher in the geologic column some of these conglom¬ 
erates greatly resemble the conglomerates at the base of the Semi- 


FRANCIS FORMATION 


115 


nole in the type area of that formation. For that matter, however, 
they also closely resemble the conglomerates of the Wewoka, Hold- 
enville, and Vamoosa formations, and were it not for the presence 
of arkose in the Pontotoc strata, hand specimens of Francis con¬ 
glomerate could probably not be distinguished from similar speci¬ 
mens of the chert conglomerates in that terrane. All the very simi¬ 
lar chert conglomerates in the Pennsylvanian section must have 
had a similar source. The writer is in agreement with Taff’s 72 
suggestion that this source was the Ouachita area. 

The upper part of the Francis formation is a shale that is about 
100 feet thick. This part carries a few thin sandstones and one 
rather persistent conglomeratic limestone. The limestone is often 
very fossiliferous and is typically exposed in the road about 100 
yards west of the school house in the southeast corner of sec. 19, 
T. 6 N., R. 7 E. In the vicinity of Ada this shale and a part of the 
underlying sandstone member is overlapped by the Ada formation. 
Southwest of Ada successively lower beds are overlapped until in 
the vicinity of Fitzhugh the entire formation is concealed by the 
Ada formation. 


FOSSILS 

The Francis formation carries its most prolific fauna in the 
thick shale series which is quarried at the Ada brick plant. At the 
latter point 50 well preserved species were collected. 

AGE AND CORRELATION 

The Francis formation is thought to be equivalent to the Pueb¬ 
lo and lower Moran of Texas, and to the Shawnee and lower 
Wabaunsee of Kansas and Missouri. 

STRUCTURE 

From Ada to the northern edge of the quadrangle the Francis 
has a normal dip of 100 feet per mile. The direction of dip is 65° 
west of north. From Ada westward to the center of T. 3 N., R. 
5 E. the dip is almost directly north, while between the latter points 
and Fitzhugh it is again toward the northwest. 

In addition to beds of the upper Seminole formation, the fault 
in sec. 13, T. 3 N., R. 5 E., also cuts the lower strata of the Francis. 

About three miles northwest of Oakman is a down- 
dropped fault block. The direction of the limiting faults is north¬ 
west-southeast and they cut not only Francis, but also succeeding 
Belle City and Vamoosa strata. Southeastward toward Oakman 
the faults die out, their extension being marked by down-folding of 
strata so that a westward plunging syncline is produced in the area 
intervening between them. 


72 U. S. Geol. Survey, 19th Ann. Rept. 3, p. 442, 1899. 



Fauna of the Francis J or motion 


116 


FRANCIS FORMATION 


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FRANCIS FORMATION 


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Fauna of the Francis formation—Continued 


118 


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FRANKS CONGLOMERATE 


119 


ECONOMIC IMPORTANCE 

Except in the manufacture of brick at Ada, the Francis for¬ 
mation has no commercial use. The dark organic shales with 
associated beds of coarse and porous sandstones suggest that in 
favorable areas the formation might yield commercial quantities of 
oil or gas. This possibility is somewhat strengthened by two known 
outcrops of asphaltic sandstone that occur within the formation. 

One outcrop occurs almost two miles west of Sasakwa where 
the road on the east-west half section line is crossed by a little 
stream. This is in the west central part of sec. 34, T. 6 N., R. 7 E. 
The other outcrop is in the road about one-fourth mile east of 
Oakman. 


FRANKS CONGLOMERATE 

NAME 

Franks conglomerate is a term given by Taff 73 to a series of 
limestone conglomerates exposed in and around the Arbuckle Moun¬ 
tains. The name is after the town of Franks which is located in 
sec. 34, T. 2 N., R. 6 E. 

AREAL DISTRIBUTION 

In discussing the Franks conglomerate Taff 74 describes its 
areal distribution as follows: 

A broad belt of this conglomerate extends across the northwestern 
part of the Arbuckle Mountains to the vicinity of Franks in the adjoining 
Stonewall quadrangle. From the northwest corner of the Tishomingo quad¬ 
rangle northeastward it crosses the eroded edges of the Ordovician, Upper 
Silurian, and Devonian formations. From a nearly flat position on the Hun- 
ton limestone near Franks it extends southeastward unconformably across 
the Woodford chert and Caney shale to a position above the latter in the 
Carboniferous section. 


THICKNESS AND CHARACTER 

In the vicinity of Franks, conglomeratic strata are exposed 
through a section of approximately 1,500 feet. Many of the beds 
are fossiliferous, and (contrary to Taff’s statement, as given above, 
that the Franks conglomerate of this area is nearly flat) all are 
highly folded and locally faulted. The conglomerates are largely 
composed of limestone fragments which vary in size up to a diam¬ 
eter of four or five inches. Toward the east and northeast the 
fragments diminish in size and quantity within any given stratum; 
the beds becoming sandy or grading into shale in these directions. 

73 Taff, J. A., U. S. Geol. Survey, Geol. Atlas, Tishomingo Folio, No. 98,1903. 
74 Idem p.5 



120 


FRANKS CONGLOMERATE 


The conglomerates near Sulphur, in the southwestern part of 
the Stonewall quadrangle and in the northwestern part of the Tish¬ 
omingo quadrangle, are also chiefly made up of limestone frag¬ 
ments that are similar to those which constitute the beds at Franks. 
The lithologic similarity of the limestone fragments at Franks and 
Sulphur, and the fossils contained within the fragments clearly indi¬ 
cate a common source (the Arbuckle Mountains) for the conglomer¬ 
ates in the two areas. The resemblance of the strata in the two 
localities led Taff to the conclusion that the conglomerates at Franks 
and Sulphur were contemporaneous equivalents. 


AGE AND CORRELATION 

After correlating, under the formation name Franks, the 
several outcrops of limestone conglomerates that occur in the region 
of the Arbuckle Mountains, Taff 75 concluded that they occupied a 
a position near the base of the Pennsylvanian series and graded 
eastward into the Wapanucka limestone. Taff was followed in this 
correlation by Reeds 76 and Wallis 77 who did later work in the 
Arbuckle area. Still later Moore 78 and McCoy 79 published papers 
in which a correlation of the Franks conglomerate with the Semi¬ 
nole conglomerate was advocated. Weidman 80 did work in the re¬ 
gion of the conglomerates in connection with his studies of evidences 
of glaciation in the Arbuckle region. In the course of his work he con¬ 
cluded that the Franks conglomerate forms a series of conglomerate 
beds reaching from the base up to higher horizons of the Pennsyl¬ 
vanian and probably into the basal Permian. 

The conclusions of Moore and McCoy were quite different 
from the earlier conclusions; for v/hereas the Wapanucka lime¬ 
stone, which Taft, Reeds, and Wallis considered as equivalent to the 
Fianks, is near the base of the Pennsylvanian, the Seminole forma¬ 
tion is near the top of the series. Weidman’s conclusion also dif¬ 
fers widely from earlier opinions. The wide divergence of opinion, 
as regards the correlation of the limestone conglomerates of the 


75 Idem p. 5 

‘ G Reeds, Chester A., A report of the geological and mineral resources of the 
Arbuckle Mountains, Oklahoma: Okla. Geol. Survey Bull. 3, i9io. 

“ Walks, B Franklin, The geology and economic value of the Wapanucka 
limestone of Oklahoma: Okla. Geol. Survey Bull. 23, 1915 . * 

78 Moore, Raymond C., Folding in southern Oklahoma oil fields: Am. Assoc. 
Pet. Geologists, vol. 5, no. l, 1921 . 


‘•McCoy, Alex. W., A short sketch of the paleogeography and historical geo¬ 
logy of the Mid-continental district and its importance to petroleum geology: 
Bull. Am. Assoc. Pet. Geologists, vol. 5, No. 5, 1921 . 

80 Weidman, S., Evidence of glaciation in the Arbuckle Region: Proceedings of 
the Okla. Acad. Science p. 73, 1922. 



CONGLOMERATES AT SULPHUR 


12! 


Arbuckle region, in itself establishes the fact that the conclusions 
of at least some of the authors are incorrect. In the course of the 
present investigation therefore, considerable time was devoted to 
the problem of correlating the Franks conglomerate. 

The beds in the type area were followed eastward and in that 
direction were found to be tracable, no-t into the Wapanucka lime¬ 
stone as reported by Taff, out into the McAlester, Savanna, and 
Boggy formations. The YVapanucka limestone was found to emerge 
from beneath the conglomerates at a point about two miles south¬ 
east of the town of Franks. 

Northwestward from Franks there are several hundred feet 
of conglomeratic strata that are confined to the western end of the 
Franks graben. These strata are higher in the section than those 
which are tracable into the McAlester, Savanna, and Boggy forma¬ 
tions and, since the outcrops of these higher beds do not extend 
outside of the western end of the Franks area, their correlation 
rests on the evidence afforded by paleontology and lithology. Near 
the base of this higher portion of the Franks conglomerate 
is a thick, brown sandstone that agrees closely as to color, thick¬ 
ness, texture, ard contained fossils with a sandstone that, in the 
northern part of the Stonewall quadrangle, marks the top of the 
Wewoka formation. The suggested correlation is supported by 
faunal evidence that is contributed by a zone that occurs in the 
Franks section somewhat above the sandstone just mentioned. Fos¬ 
sils from this zone include several forms that are characteristic of 
the Holdenville formation. Near the top of the geologic section of 
the western Franks area is a thick shale that is very similar, both 
as to lithologic character and contained fossils, to the thick shale 
that occurs at the base of the Francis formation. 

These several lines of evidence strongly suggest the correla¬ 
tion of the upper part of the conglomeratic strata of the Franks 
area with the upper Wewoka, Floldenville, Seminole, and Francis 
formations. Under the discussions of these several formations the 
evidence here cited is treated in more detail. 

CONGLOMERATES AT SULPHUR 

As stated previously all earlier writers on the Arbuckle area 
correlated the conglomerates at Franks with the conglomeratic 
strata exposed near'the town of Sulphur. Upon investigation, how¬ 
ever, it was found that the outcrop of the conglomerates near Sul¬ 
phur are continuous northward with the outcrops of beds in the 
Vanoss formation. The Vanoss formation constitutes the top of 
the Pennsylvanian series in the Stonewall quadrangle. The forma¬ 
tion is definitely characterized by the abundance of arkosic material 
which it contains. 


122 


CONGLOMERATE AT SULPHUR 


There is no arkosic material in any of the strata of the Franks 
area and the areal mapping, done in connection with the present 
work, establishes the fact that the Vanoss formation is much 
younger than the uppermost strata of the type Franks. It is ob¬ 
vious, therefore, that the conglomerates at Sulphur cannot be cor¬ 
related with the conglomerates at Franks. Aside from the fact that 
the conglomerates at Sulphur are tracable into a formation that is 
much younger than any of those with which the Franks conglomer¬ 
ates may be correlated, the strata in the two areas have the follow¬ 
ing physical differences: 

Franks Conglomerate Vanoss Formation 

Which includes conglomerates at 

1. Non-arkosic. Sulphur 

2. Highly folded and faulted. Arkosic. 

_ P .. ... 2. Slightly folded. 

3. Fossils common, with numerous 3 Fos s si , s scarce , with few species. 

species. 

When the Vanoss formation was mapped northward the writer 
found that the basal contact of that formation passes about eight 
miles west of the type area of the Seminole formation. 

POSSIBILITY OF CORRELATING THE CONGLOMERATES AT SULPHUR 
WITH THE SEMINOLE CONGLOMERATE 81 . 

Elsewhere in this report the Seminole formation is discussed in 
detail. It was named and defined by Taff 82 who gave its thickness 
as “about” 150 feet. The type area is located in the northwest 
corner of the Coalgate quadrangle and adjoins the northeast corner 
of the Stonewall quadrangle. In this region the formation dips 
westward at an average angle of one degree. Farther westward the 
dip decreases slightly, but there is no doubt that in the distance 
intervening between the Seminole type area and the nearest point 
of the Vanoss outcrop (this point is about eight miles west of the 
Seminole type area) a thickness of more than 500 feet of sedi¬ 
ments is exposed. The conditions outlined permit no possibility of 
a correlation of any part of the Vanoss formation with any part 
of the type Seminole. 

CONCLUSIONS 

1. The conglomerates at Franks and Sulphur are distinctly 
different in age and not to be correlated. 

2. The lower part of the Franks conglomerate of the type 

81 This discussion is included under the treatment of the Franks conglomerate 
because of the correlation, advocated by Moore and McCoy of the Franks and 
Seminole conglomerates. 

82 Taff, J. A., Geol. Survey Geol. Atlas, Coalgate Folio, No. 74, 1901. 



BELLE CITY LIMESTONE 


123 


area is equivalent to parts of the McAlester, Savanna, and Boggy 
formations, The upper part of the Franks conglomerate, of the 
type area, is to be correlated with parts of the Wewoka, Holden- 
viile, Seminole, and Francis formations. 

3. It is thought advisable to abandon the term Franks con¬ 
glomerate and to refer to the conglomeratic strata of the Franks 
area by the names of the several formations which the section there 
is known to include. If the term Franks is retained it should be 
restricted to the strata in the type area around Franks, and to those 
Pennsylvanian limestone conglomerates of the Arbuckle region that 
are (a) fossiliferous, (b) highly folded or faulted and (c) non- 
arkosic. 

BELLE CITY LIMESTONE 

NAME 

Belle City limestone is the manuscript name given by Boone 
Jones 83 to a formation that is well developed in the Stonewall quad¬ 
rangle. The name is after Belle City, a village in Seminole County. 

AREAL DISTRIBUTION 

The exposure of this formation is limited to the northern half 
of the Stonewall quadrangle. The main outcrop extends from the 
northwest corner of sec. 18, T. 6 N., R. 7 E., southwestward to a 
point just east of Byng and is there covered by Guertie sand. 

West of the section house about one-fourth mile south of Byng 
is a small outlier of the formation and a few hundred yards 
south of this is the northern end of another and larger mass that 
is not visibly connected with the main outcrop. The south end of 
this probable outlier is covered in part by Guertie sand and is over¬ 
lapped by the Ada formation. 

The formation is well exposed almost everywhere along the 
trend of the outcrop. It is more resistant than the underlying shales 
of the Francis formation, with the result that the contact of the two 
formations is generally marked by a steep, prominent, eastward¬ 
facing escarpment. The Belle City limestone has its greatest thick¬ 
ness and what is probably its best exposure on the south bluff of 
Canadian River in sec. 15, T. 5 N., R. 6 E. 

THICKNESS AND CHARACTER 

The formation has an average thickness of 30 feet. It is com¬ 
posed of two limestones of varying thickness with an intervening 
shale. The upper lime is generally thicker and much more massive 
than the lower. Its range in thickness is from one foot, as just 
south of Byng, to as much as 15 feet near Canadian River. The 
bed is white or light gray in color and is often characterized by well 
developed styliolites." Pronounced weathering along joint cracks is 

83 Jones, Boone, Unpublished manuscript prepared fer the Okla. Geol. Survey, 
1922. 



124 


BELLE CITY LIMESTONE 


Fauna oj the Belle Citx limestone 


SPECIES 


BRYCZOA 


Fenestella spinulosa. 

Polvpora nodocarinata 


BP ACIIIOPODA 


Composita subtilita.... .. 
Meekella striatacostata 

Productus sp. 

Productus cora... 

Productus insinualus_ 

Spirifer cameratus.. 


PELECYPODA 


Allorisma sp........ 

Aviculopecten occidentalis... 

Myalins cf. recurvirostris.... 

Myalina recurvirostris sinuosa. 

Pinna peracuta.. 

Pleurophorus sp. . . 

Pseudomonotis radialis.... 

Schizodus meekanus. 


GASTROPODA 


Bellerophon sp..... 

Euphemus carbonarius... 

Euphemus nodocarinatus... 

Loxonema ? sp. 

Naticopsis remex... 

Pleurotomaria monilifera_- 

Sphaerodoma intercalaris.. 

Sphaerodoma ponderosum... ... 

Sphaerodoma primigenium... 

Strophostylus nana..... 

Worthenia tabulata .. 


CEPHALOPODA 


Coloceras liratum... 

Metacoceras cornutum...... 

Orthoceras sp... 

Pseudorthoceras knoxense. 

Schistoceras fultonense.... 

A—abundant. C—common. B—rare. 


LOCALITIES 


184 


225 


R 

R 


. R 

C 

R 

. R 

C 

A . 



I 


R 

C 

R 

.. A 

R . 

R 

R 

R 


R 

R 

R 

A 

C 

R 

R 

R 

C 


R 


A 

R 


R 

a. 





















































VAMOOSA FORMATION 


125 


common and in the eastern part of sec. 24, T. 6 N., R. 6 E., results 
in the formation of small sink-holes at the intersection of a few of 
the prominent joints. 

The lower limestone bed is buff colored. Its range in thick¬ 
ness is from one foot, as in the vicinity of Byng, to as much as five 
feet near Canadian River and northward. At variance with the 
massive character of the upper member of the formation the bed¬ 
ding of this stratum is relatively thin. 

The interval between the upper and lower limestones is com¬ 
posed of shale that ranges in color through shades of green, blue, 
and black. Its average thickness is 12 feet. 

FOSSILS 

All three members of the formation are fossiliferous, but the 
largest fauna is from the massive limestone at the top. The species 
identified from the several collections taken from the different 
members are given in the accompanying chart. 

AGE AND CORRELATION 

The Belle City limestone is to be correlated with at least a part 
of the Moran of Texas, and is equivalent to a part of the Wabaun¬ 
see of Kansas and Missouri. 


STRUCTURE 

The average dip of the formation is one degree. The direc¬ 
tion of normal dip is 70 degrees west of north. 

VAMOOSA FORMATION 

NAME 

A suitable geographic name was not available for this forma¬ 
tion. The term finally selected is after the village of Vamoosa 
which is located in the northern part of the Stonewell quadrangle, 
about one-half mile west of the outcrop. The formation is typically 
developed on the main road between Sasakwa and Konawa. 

AREAL DISTRIBUTION 

In the Stonewall quadrangle the formation is exposed over an 
area of approximately 20 square miles. The lateral extent of its 
outcrop is similar to that of the underlying Belle City limestone. 
From the northern edge of the quadrangle, the principal outcrop 
trends in a southwesterly direction to an area about one-half mile 
east of Byng and is there covered by Guertie sand. South of Byng 
the formation is exposed on what is believed to be an outlier. The 
southern part of this exposure is covered in part by Guertie sand 
and is overlapped by the Ada formation. 

THICKNESS AND CHARACTER 

Where all of the formation is exposed the entire section has 


126 


VAMOOSA FORMATION 


an everage thickness of 260 feet. At the base is about 30 
feet of dark shale that might easily be mapped as a separate forma¬ 
tion. No collections were made from this member, but it is very 
probably fossiliferous. The main mass of the formation is above 
this shale and has a maximum thickness of about 230 feet. It 
consists in large part of chert conglomerates, (Plate XVI—A and B) 
of massive, coarse, red and brown sandstones, and red shales. 
The clastic material is finer near the top and the red coloration is 
there also less pronounced. 

The chert conglomerates of the Vamoosa formation closely 
resemble those of the Wewoka, Holdenville, Seminole, and Francis 
formations, but may be distinguished from somewhat similar beds 
in the Pontotoc terrane because of arkosic material contained in 
the latter. The Vamoosa formation contains a greater thickness of 
chert conglomerates than does any other formation of the area. It 
is probably to the beds of this formation that McCoy 84 referred as 
“the main horizon in a series of conglomerates.” The chert frag¬ 
ments which make up the conglomerates are mostly angular and 
range in size from a fraction of an inch to as much as three inches 
in length. The average length, however, is less than an inch. 

Overlap of the Vamoosa formation, by the succeeding Ada 
formation, is progressive southward. For this reason only the lower 
shale and about 30 feet of the clastic portion of the formation are 
exposed near Byng. 

No fossils were found nor is it highly probable that any are 
present in the clastic beds of the Vamoosa. 

AGE AND CORRELATION 

Because of the absence of collections from the Vamoosa for¬ 
mation and the paucity of fossils in the succeeding Ada formation 
and the still higher Pontotoc terrane, the problem of correlating 
the Vamoosa and later strata is very difficult. As stated eleswhere, 85 
the method used in determining the correlations here suggested are 
largely based on the percentage and average range of common 
species. 86 

The evidence derived from a strict application of this method 
to the Vamoosa and Ada formations, as well as to the strata of the 
Pontotoc terrane, is conflicting and contradictory. The general 
weight of evidence, however, seems to favor a correlation of the 
Vamoosa with the lower Putnam of Texas, and with a portion of 
the Wabaunsee of Kansas and Missouri. Evidence supporting this 

s *McCoy, A. W., Am. Assn. Pet. Geologists, vol. 5, Footnote on p. 546, 1921 . 
85 See page 156. 

Sfi Only four classes of invertebrates (Brachiopoda, Pelecypoda, Gastropoda 
and Cephalopoda) were used in this calculation. 



PLATE XVI 



A. DETAIL OF MISSIVE CHERT CONGLOMERATE, CHARACTERISTIC OF 
A LARGE PART OF THE VAMOOSA FORMATION 



B. GENERAL VIEW OF CHERT CONGLOMERATE IN THE UPPER PART OF 
THE VAMOOSA FORMATION IN SEC. 26, T. 6 N., R. 6 E. 







128 


ADA FORMATION 


correlation is contributed by two collections of plant fossils from the 
Pontotoc terrane. The plants indicate that the Pennsylvanian- Per¬ 
mian contact lies near the top of the Vanoss formation of the Pon¬ 
totoc terrane. 


STRUCTURE 

The normal dip of the formation agrees with that of the Belle 
City limestone. That is, it averages about one degree and is in a 
direction about 70 degrees west of north. The block fault east of 
Byng is discussed in the treatment of the Francis formation. 

ADA FORMATION 

NAME 

The formation is here named after the town of Ada within and 
to the west of which lies the type area. 

AREAL DISTRIBUTION 

The outcrop of the Ada formation extends from the northern 
edge of the Stonewall quadrangle, north of Vamoosa, southwest- 
ward to a point about three miles southeast of Roff where it is over¬ 
lapped by the Vanoss formation of the Pontotoc terrane. In the 
valley of Canadian River, north of Tyrola, the formation is covered 
in part by Guertie sand of Pleistocene age, and in part by recent 
river sand. 


THICKNESS AND CHARACTER 

The average thickness of the Ada formation is about 100 feet. 
Limestone conglomerates and coarse sandstones are very promin¬ 
ent along the greater portion of the outcrop. Clastic material be¬ 
comes less toward the north, however, and in the vicinity of 
Vamoosa is very scarce. With the decrease in the amount of clas¬ 
tic material northward the formation becomes thinner and at the 
northern edge of the sheet has a total thickness of only about 60 
feet. 

One very characteristic feature of the formation is the asphalt 
which it contains. This is always associated with the conglomerates 
or coarse sandstones many of which are often highly saturated. 
One mile west of Ada, asphalt-bearing sandstones and conglomer¬ 
ates are quarried for paving purposes. 

North of Canadian River exposures of asphaltic strata are less 
numerous than they are to the south, but such strata are often 
encountered in water wells. 

The presence of asphalt in the Ada formation is not easily ex¬ 
plained. The shales of the formation are mostly of light colors and 
seem to offer slight possibility as a source of the material. That 


ADA FORMATION 


129 


the asphalt was derived from organic material within the clastic 
beds which it saturates is also negatived by the paucity of fossil re¬ 
mains within those strata. The asphalt has not migrated from 
underlying or overlying strata as is shown by its absence in adjacent 
formations. Several of the older formations exposed in the Ar- 
buckle Mountains carry oil and asphalt saturated beds, and in the 
absence of any other explanation it is possible that the asphalt of 
the Ada formation has been derived from these sources. The 

Simpson formation in particular has several rich asphaltic sands 

which in the region southwest of Sulphur are extensively quarried 

for paving. Within the conglomerates of the Ada formation there 

are many fragments which contain Hunton and Viola fossils, while 
the sand which composes the sandstone strata is very similar to 
that in the Simpson. This evidence shows clearly that the Ar- 
buckle Mountains were the source of at least a great part of the 
sediments that make up the Ada formation, and it occurs to the 
writer that as the sediments were carried out from the mountains 
and deposited, heavy oil from the exposed asphaltic sands of the 
Simpson might also have been brought out and deposited. Such an 
explanation has been used to account for some of the oil deposits of 
India. 87 

Although fossils are very scarce in the Ada formation a few 
species were found which indicate that the sediments are of marine 
origin. This being the case the objection seems plausible that any 
oil which accompanied sediments from the mountains would have 
been washed out and carried away before the sediments were finally 
deposited. An inconclusive experiment was made to test this pos¬ 
sibility. A tank was constructed and placed on an inclined axle s@ 
that it could be revolved. (Plate XVIII). The tank was then part¬ 
ially tilled with powdered asphaltic sand from the Simpson forma¬ 
tion and to this was added several pebbles so that when the tank 
was revolved a pounding or crushing process somewhat analogous 
to shore conditions could be produced. Arrangements were then 
made so that a continuous stream of water could be circulated 
through the tumbling sand and pebbles. By means of a belt and 
pulley the axle of the tank was then connected with a line shaft in 
a machine shop and allowed to rotate an average of 12 hours per 
day for one month. When at the end of this time the tank was 
opened it was found that about one-third of the oil had been washed 
away by the circulating stream of water and that most of what re¬ 
mained was contained in rounded balls of sand that had been pro 
duced by the revolution of the tank. 

The experiment is inconclusive because of the factor of time, 


87 Stuart, Murray, The sedimentary deposition of oil: Rec. Geol. Survey India 
vol. 40 p. 320. 1910. 



130 


ADA FORMATION 


but upon examination a few rounded balls of sand, very rich in as¬ 
phalt, were found in the conglomeratic beds of the Ada formation. 

Near the base of the formation is a thin black limestone that 
is very persistent in the vicinity of Ada. 


PLATE XVII 



A. LIMESTONE CONGLOMERATE IN THE ADA FORMATION, ONE-HALF 

MILE WEST OF ADA. 



B. ASPHALTIC SANDSTONE IN THE ADA FORMATION 
LOCATION, ASPHALT PIT ONE MILE WEST OF ADA. 


North of Canadian River the Ada formation appears to rest 
conformably upon the Vamoosa, but toward the south it overlaps 
several of the underlying formations. 

About one mile south of Byng the Vamoosa formation is over- 









ADA FORMATION 


1*1 


lapped, and in the vicinity of Fitzhugh the Ada formation extends 
across the Francis and Seminole formations to an unconformable 
contact with the Viola limestone. 

PLATE XVIII 



APPARATUS USED IN WASHING ASPHALTIC SANDS OF THE SIMPSON 

FORMATION. 


FOSSILS 

One collection of invertebrate fossils, doubtfully from the Ada 
formation at locality 188, afforded the following species. 

Bellerophon crassus 
Schizostoma catilloides 
Pharkidono us percarinatus 
Productus sp. 

Pseudorthoceras ? cf. knoxense 
Schizodus sp. 

Sphaerodoma ? sp. 

Spirifer cameratus 

This collection is from near the unconformable contact of the 
Ada and Francis formations and, since the contact at that point is 
not clear, may be from the latter formation. 

Several specimens of Catamites sp. and Cordiates cf. communis 




132 


PONTOTOC TERRANE 


were taken from the asphalt pit west of Ada. A few specimens re¬ 
sembling Soleniscus newberryi were also secured here. The black 
limestone near the base of the formation carries Soleniscus newberryi 
and Bulimorpha of inornata. 

AGE AND CORRELATION 

These few faunules indicate a Pennsylvanian age for the Ada 
formation. The Belle City limestone which normally occurs more 
than 250 feet below the base of the Ada is apparently equivalent 
to the Moran of Texas, and a portion of the Wabaunsee of Kansas, 
and Missouri. Meager faunal evidence from the Pontotoc terrane 
indicates that the Pennsylvanian-Permian contact occurs about 500 
feet above the top of the Ada. A consideration of this general evi¬ 
dence suggests a correlation of the Ada with a part of the Putnam 
of Texas, and with an upper portion of the Wabaunsee of Kansas, 
and Missouri. 


STRUCTURE 

The normal dip of the Ada formation is toward the northwest. 
The dip amounts to an average of 90 feet per mile. In the gas 
field north of Ada is a small amount of local folding that apparently 
controls the gas accumulation there. 

ECONOMIC IMPORTANCE ' 

The asphaltic sands and conglomerate beds west of Ada are 
intermittently quarried for paving purposes. 

PONTOTOC TERRANE 

NAME 

The Pontotoc terrane takes its name after Pontotoc County 
in the western part of which it is typically developed. In earlier 
papers 88 this division was referred to as a series. It now appears, 
however, that it is of both Pennsylvanian and Permian age, so that 
the term series is less applicable than is the term terrane. 

AREAL DISTRIBUTION AND CHARACTER 

The Pontotoc was first described 89 as a series rather than as a 
formation for the reason that although most of the sediments with¬ 
in it are similar, in that they contain a varying quantity of arkosic 
material, there are three rather distinct divisions that themselves 
may be mapped as formations. These are here described, beginning 
with the lowest one, as the Vanoss formation, the Stratford forma¬ 
tion, and the Konawa formation. The lower part of the Konawa 


88 Morgan, Geo. D., Okla. Geol. Survey Circulars 10, 11 and 12, 1922-1923. 
89 Morgan, Geo. D., Okla. Geol. Survey Circular 11, 1922. 



VANOSS FORMATION 


133 


formation possibly (but improbably) represents merely a north¬ 
ward graditional facies of the Vanoss and Stratford formations. 

The Pontotoc strata are generally arkosic; strongly so in the 
lower portion, but becoming less and less so at higher horizons. 
In the beds west of Asher (Asher formation) arkosic material is en¬ 
tirely lacking. 

The source of a large part of the material comprising the Pon¬ 
totoc formations was the Arbuckle Mountains. This is particularly 
indicated by the limestone fragments contained in the strata. Many 
of these carry Hunton and Viola fossils, and were clearly derived 
from those horizons. It is thought that all the igneous material 
contained in the Pontotoc beds was derived from the Arbuckles. In 
this material the grains of quartz and feldspar are usually distinctly 
separated and are often of large size. Even in outcrops remote from 
the mountains it is not unusual to find great numbers of well pre¬ 
served orthoclase crystals entirely free from quartz and averaging 
as much as one-fourth inch in length. This evidence is taken to in¬ 
dicate that periods of uplift and torrential distribution of these ma¬ 
terials alternated with long quiescent periods during which the con¬ 
tributing igneous mass weathered and crumbled in situ. 

The areal exposure of the three formations covers a large por¬ 
tion of the western half of the Stonewall quadrangle. 

The Pontotoc terrane lies between the Ada and Asher forma¬ 
tions, and in the Stonewall quadrangle has an average thickness of 
from 1,200 to 1,500 feet. 

In the Stonewall and adjacent areas only one small outcrop is 
known, where igneous material is present in sediments older than 
the Pontotoc. This exception is in the base of the Wewoka forma¬ 
tion southwest of Allen. From these data the conclusion is drawn 
that small isolated peaks of igneous material may have been ex¬ 
posed in the Arbuckle area as early as Wewoka time and that by 
early Pontotoc tim£ the thick covering of early Paleozoic sediments 
was so far removed from the crest of the Arbuckle Mountains that 
the igneous core was exposed over considerable areas. 

DIVISIONS 

VANOSS FORMATION 

NAME 

The name of this formation is alter the town of Vanoss which 
is situated on the outcrop in the north central part of T. 3 N., R. 4 E. 

THICKNESS AND CHARACTER 

The Vanoss formation consists of alternating sandstones, con¬ 
glomerates, (Plate XIX) shales and a few thin limestones. All 


134 


VANOSS FORMATION 


the strata are arkosic, some of the sandstones so much so that at 
first glance a few of them might be mistaken for true granites. 

The base of the Vanoss rests on the Ada formation, the con¬ 
tact between the two being the plane dividing the arkosic and non- 
arkosic materials. 90 Due to the lenticular nature of strata along the 
contact and to the fact that the Vanoss is progressively overlapping 
southward no one stratum can be selected to mark the adjacent 
limits of the formation. The base of the arkosic zone, however, is 
relatively contemporaneous. The resistant sandstones of the lower 
part of the formation form Lightning Ridge east and south of 
Vanoss. 

Near the center of the formation there are several thin lime¬ 
stone beds. These were not observed north of Canadian River, 
but appear intermittently along the outcrop to the south of that 
stream. They are generally argillaceous and are subject to rapid 
gradation into shale. Where freshly exposed the limestones are 
light gray in color and relatively soft, but on weathering become 
hard and white. Several of these beds are well exposed at the east¬ 
ern edge of the town of Center. Good exposures are also common 
in the region about one mile east of Vanoss. The limestones are 
less arkosic than the associated sandstones, but some of them carry 
an appreciable amount of feldspathic fragments. 

In the upper part of the Vanoss formation sandstones are less 
prominent than they are near the base. The shales which consti¬ 
tute the greater part of this upper portion are generally of light 
color, ranging through shades of green and gray. Occasional red 
shales are also present. With the decrease in sandstone there is 
also a decrease in the quantity of arkose. Locally, however, there 
are beds that are almost entirely composed of this material. 

The upper limit of the Vanoss formation is marked by the base 
of the Hart limestone member of the Stratford formation. The 
thickness of the Vanoss formation increases southward. The ex¬ 
posed portion east of Konawa totals only about 2 50 feet, while near 
the southwest corner of the quadrangle there are about 650 feet of 
strata within the formation. 

AGE AND CORRELATION 

The shales that occur above the limestones near the center of 
the formation carry plant fossils. A collection taken from the gullv 
that drains northward from the town of Center (locality No. 178) 
was sent to Mr. David White who was able to identify the following 
species: 


90 In the sediments of the Stonewall quadrangle and closely adjoining areas 
only one locality was found where igneous material was present in beds below 
the base of the Vanoss formation. This is in the Wewoka formation south¬ 
west of Allen. (See discussion of the Wewoka formation) 



PLATE XIX 



A. MASSIVE ARKOSIC SANDSTONE IN THE VANOSS FORMATION, 

IN SEC. 29, T G N., R. 6 F. 



B RIMESTONE CONGLOMERATE IN THE VANOSS FORMATION, 

One mile east of Sulphur. This bed carries a small amount of arkosic material 





136 


VANOSS FORMATION 


Neuropteris ovata, the large form of upper Pennsylvanian 
age; 

Pecopteris arborescens 

Pecopteris hemitelioides; fragments of Cordaites, and prob¬ 
ably C. communis; indeterminable stem fragments possibly 
belonging to a fern; a few small fragments of a large 
species of Pecopteris comparable to P. (“Callipteridium”) 
dawsonianum, or one of the closely related species from the 
Conemaugh and Dunkard of the Appalachian trough; and 
a fern fructification, probably a new species, if not a new 
genus. 

From the evidence afforded by this collection Mr. White con¬ 
cluded that although the plants were strongly suggestive of the 
Permian it was his opinion that they were indicative of a very late 
Pennsylvanian age. 

In the section line one-half mile north of Beebe, (Locality No. 
210) a single plant fossil was found which was identified as Walchia 
piniformis. This fossil also was sent to Mr. White who kindly gave 
the opinion that the plant, although a Walchia , is not clearly of the 
species W. piniformis. He stated, however, that it is comparable to 
that species. 

In later communication Mr. White stated that: “Walchia can 
be but little if any earlier than the base of the Permian” and again, 
“there are a number of cases in which it will be clear that Walchia 
is present in the uppermost horizons of the Pennsylvanian. Yet it 
is in general so characteristic of the Permian that each such case 
deserves special inquiry 91 .” 

The sandestone from which the Walchia was secured is near 
the top of the Vanoss formation and is at least 100 feet above 
the plant bearing shales at Center. 

In the Beebe area and at two places northwest of Center 
is a thin fossiliferous limestone that occurs in the section about half 
way between the two plant-bearing zones. Along the eastward facing 
bluff in sec. 18 T. T. 5 N., R. 5 E., the limestone is well exposed and 
there yielded the following species: 

Bellerophon bellus 
Myalina recurvirostris 
Naticopsis altonensis 
Naticopsis sp. 

Pleuratomaria arenaria 
Productus cora 
Schizodus sp. 

Sphaerodoma texanus 
Yoldia glabra 


91 Personal communication. 



STRATFORD FORMATION 


137 


This faunule, although mostly composed of species that ex¬ 
tend into the Permian is strongly suggestive of Pennsylvanian age. 
Northwest of Center a lithologically similar bed with essentially the 
same fauna outcrops in the southeast corner sec. 12, T. 4 N., R. 4 E., 
In the west central part of section 15, of the same township, is an 
outcrop of a limestone that also strongly resembles the bed in ques¬ 
tion. It is thought that these outcrops are of the same limestone 
and that it is to be correlated with the bed exposed north of Beebe. 
Along the eastward facing bluff in sec. 9, T. 3 N., R. 5 E., just above 
the base of the Vanoss formation, is a calcareous sandstone which 
carries a few poorly preserved specimens of Bulimorpha. These, are 
comparable to the species B . inornata. 

The fossils that have been mentioned represent all that were 
found in the Vanoss formation. The rather fragmentary evidence 
which they afford and the relation of the formation to lower beds 
constitutes the grounds on which must be based the conclusion as 
to the age of the Vanoss formation. 

The Belle City limestone, which is the first abundantly fossil- 
iferous zone below the Vanoss formation, is thought to be equiva¬ 
lent to the late Pennsylvanian of Texas, Kansas, and Missouri. If 
the fossil plants from near Center, although somewhat indicative of 
Permian, are in reality of Pennsylvanian age; if the fossiliferous 
limestone from which the collection was taken northeast of Beebe 
is also of Pennsylvanian age, and if the Walcliia cf. piniformis is 
strongly indicative of a Permian age for the stratum from which it 
was derived, it appears that the lower part of the Vanoss formations 
is of Pennsylvanian and that the uppermost part is of Permian age. 
This being the case it is reasonable to suppose that with the depos¬ 
ition of the highest beds of the Vanoss formation the Permian per¬ 
iod had been fully initiated. The base of the Hart limestone mem¬ 
ber of the Stratford formation is therefore taken as the contact be¬ 
tween the Pennsylvanian and Permian Systems. 

The Vanoss'formation is probably equivalent to the upper Put¬ 
nam of Texas, and to the late Wabaunsee of Kansas and Missouri. 

STRATFORD FORMATION 

NAME 

The name of this formation is after the town of Stratford 
which is situated in the western part of the Stonewall quadrangle. 

THICKNESS AND CHARACTER 

At the base of the Stratford formation is a series of lime¬ 
stones which constitute the Hart limestone member. Above this 
member is an undetermined thickness largely composed of 
dark colored shales. No suitable upper limit for the Stratford for¬ 
mation occurs in the Stonewall quadrangle, and since the region 


138 


STRATFORD FORMATION 


farther west has not been investigated, none is here suggested. 
About 400 feet of the formation is exposed in the Stonewall quad¬ 
rangle. 


PLATE XX 



ARKOSIC LIMESTONE—THE HART LIMESTONE MEMBER OF THE STRAT¬ 
FORD FORMATION. 

Location, west central part of section 4, one and one-half miles west of Vanoss. 
Note the large size of the feldspar crystals in the limestone. 


The Hart limestone member is typically developed near the vil¬ 
lage of that name in the western part of T. 3 N., R. 4 E. This 
member is composed of alternating limestones, shales, and sand- 




STRATFORD FORMATION 


139 


stones. In the vicinity of Hart the limestone beds are very prom¬ 
inent, but toward the north and south some of them thin out while 
others grade into shale. For this reason the boundaries of the for¬ 
mation can not be drawn with great accuracy. Northeast of Strat¬ 
ford the Hart limestone is covered by a large area of Guertie sand. 

In the bed of a small creek, near the section line in the east¬ 
ern part of sec. 2, T. 4 N., R. 3 E., is an exposure of limestone that 
constitutes an inlier within the Guertie sand. This bed closely re¬ 
sembles the limestones of the Hart member and is thought to be¬ 
long to the upper part of that division. As a rule arkosic material 
is not abundant in the limestone beds of the Hart member. It is 
always present, however, and in a few beds constitutes a large pro¬ 
portion of the rock. The top of the eastward facing bluff about one 
and one-half miles west of Vanoss is capped by a white limestone 
that is exceptionally rich in arkosic material. (See Plate XX). Out¬ 
crops of Hart limestones that have not been long exposed to weath¬ 
ering are generally rather soft and are grayish white in color. On 
weathering the beds usually become very hard, develop a concho- 
idal fracture and attain a much lighter color. 

The shales which constitute the upper part of the Stratford 
formation were given but little attention. They contain a few sand¬ 
stones, some of which are arkosic. On the road east of Stratford 
the shales are very dark and are of the nature of gumbo. 

North of the area of Guertie sand, which covers a part of the 
region between Stratford and Canadian River, beds similar to those 
of Stratford formation are not exposed. The shales here are red, 
sandstones are more abundant, and no limestones were observed. 
The difference in character of the sediments with the contributing, 
but inconclusive, evidence afforded by the structure of the area, 
leads to the conclusion that the beds north of the Guertie sand area 
belong to a formation above the Stratford and that somewhere be¬ 
neath the cover of Guertie sand this higher formation overlaps the 
Stratford. The supposedly overlapping strata are assigned to the 
Konawa formation. 

FOSSILS 

Only a few gastropods were secured from the Stratford for¬ 
mation. These were sent to Dr. J. W. Beede for identification, but 
were reported by him to be so poorly preserved as to preclude the 
possibility of specific determination. He assigned them to the genus 
Bulimorpha. 

AGE 

From the evidence contributed by the fauna, and particularly 
by the flora, of the Vanoss formation the base of the Permian is 
drawn at the base of the Hart limestone member which is at the 


140 


KONAWA FORMATION 


bottom of the Stratford formation. Northeastward from the point 
at which the Stratford formation is thought to be overlapped by the 
Konawa formation, the Pennsylvanian-Permian line is taken to be 
represented by the base of the Konawa formation. 

KONAWA FORMATION 

NAME 

This formation takes its name after the town of Konawa 
which is located on the extreme eastern edge of the outcrop. 

PLATE XXI 



MASSIVE CHERT CONGLOMERATE IN THE KONAWA FORMATION. 

Location, on main road three miles east of Asher. 

In common with most of the strata of this formation the beds here exposed 

are slightly arkosic. 

AREAL DISTRIBUTION 

The formation constitutes the upper part of the Pontotoc ter- 
rane and is exposed over more than 100 square miles in the north¬ 
west corner of the quadrangle. 

THICKNESS AND CHARACTER 

The base of this formation is drawn at the base of the typical 
red beds of the area. It was impossible to map any one stratum 
as the base of the formation so that the lower contact is only rough¬ 
ly established. In fact it is not definitely known but that the greater 



ASHER FORMATION 


141 


part of the Konawa formation is merely a northern gradational 
facies made up of parts of the Vanoss and Stratford formations. 
The general evidence of structure and lithology, however, favors 
the conclusion that it is higher than either the Vanoss or Stratford 
and that it is an overlapping formation. The Konawa formation 
is largely composed of typical red beds such as cover a large part 
of western Oklahoma. Red shales constitute the greatest thickness 
of strata in the formation, but coarse red sandstones are often 
prominent and sometimes outcrop over large areas. No limestones 
were observed in the formation. 

On the Konawa road, three miles east of Asher, is an 
outcrop of heavy chert conglomerate (Plate XXI) that resembles 
beds of the same tvpe contained by formations below the Ada. The 
only observable difference between this stratum, and those which 
occur at lower horizons, is afforded by the arkosic material which 
it contains, and which is absent from the lower strata. 

A series of coarse, red and browish-red sandstones, approxi¬ 
mately 30 feet thick, caps the north bluff of Canadian River at the 
bridge south of Asher. Beds comparable to these were not observed 
in the Stonewall quadrangle to the south of Canadian River, and it 
is thought that their outcrop passes westward beyond the limit of 
the area before crossing and emerging from the sand-filled river bed. 

From the bridge northward the outcrop of these strata forms 
a prominent eastward-facing escarpment that extends to the west 
of Asher and beyond the limits of the quadrangle about one mile 
northwest of that town. 

The upward diminishing arkosic material, common to Ponto¬ 
toc strata, entirely disappears near the base of these sandstones. In 
view of this fact and since the sandstones represent a rather defi¬ 
nite zone their basal portion is here considered as the top of the 
Konawa formation and of the Pontotoc terrane. The sandstone 
above the Konawa formation constitute the basal part of the Asher. 

The thickness of the Konawa formation is about 500 feet. 

AGE 

No fossils were found in the formaion. Its age is thought to be 
early Permian. 


ASHER FORMATION 

NAME 

Above the Konawa formation there is a continued section of 
typical red beds. The small area of these strata which outcrop in 
the extreme northwestern part of the Stonewall quadrangle are as¬ 
signed to the Asher formation which derives its name from the town 
of Asher. 


142 


GUERTIE SAND 


THICKNESS AND CHARACTER 

At the bottom of this formation is a thick series of 
coarse red sandstone that outcrop along the escarpment which ex¬ 
tends from the river bridge south of Asher to the northern edge 
of the quadrangle about one mile northwest of that town. 

The lower limit of the Asher formation probably extends south 
and west beyond the edge of the Stonewall quadrangle before cross¬ 
ing Canadian River. 

The portion of the formation present in the northwest corner 
of the quadrangle is 250 feet thick. No upper limit is here defined. 

AGE 

No fossils were found in the formation, but upon the evidence 
afforded by its color and its position in the section it is here referred 
to the lower Permian. 


GUERTIE SAND 

NAME 

This formation was named by Taff 92 after the town of Guertie 
in the Coalgate quadrangle. 

CHARACTER AND DISTRIBUTION 

In the Coalgate folio the formation is described as follows: 

Generally the sand becomes coarse downward, ending in gravel at the 
base. In many places the finer sediments have been washed away, leaving 
beds of coarse g'avel and thin mantles of pebbles. In places the deposit is 
of even texture; in other places it grades gradually from fine to coarse 
materials; and in still other places, especially noted in well sections, there a:e 
alternate strata of bluish, red, and yellow clay, silt and sand, usually ending 
at the base in quicksand or gravel. 

The sand is composed of fine white quartz which is usually more or less 
mixed with yellow silt. The pebbles of the gravel are well rounded and 
smooth, varying in size from that of a hen’s egg to a sand grain. They are 
composed of quartz, quartzite, jasper and chert, and vary in color from white 
yellow, red, and black. Very little material from the country rock such as 
limestone, shale, and sandstone, was found mixed with the gravel. 

This description is in exact accord with extensive deposits that 
occur in the northern part of the Stonewall quadrangle, and which, 
because of their similarity with the Guertie sand, are correlated with 
that formation. The largest exposure of Guertie sand in the Store- 
wall quadrangle is along the north side of Spring Creek. This 


92 Taff, J. A., U. S. Geol. Survey 19th Ann. Rept. Pt. 3, p. 439, 1899. 



GUERTIE SAND 


143 


stream follows a U-shaped course around the northern end of a 
large anticlinal uplift, and the fact that the Guertie sand conforms 
to this course raises the question as to whether the formation was 
deposited by a stream that at one time followed almost the same 

PLATE XXII 



A. ELEPHANT TUSK IN GUERTIE SAND, NEAR CENTER OT~ SOLTH 
LINE, SEC. 10, T. 3 N„ R. 5 E. 



B. GERTIE SAND, ONE-HALF MILE NORTH OF BYNG. 

course as that of the present Spring Creek, or whether it i*as depos¬ 
ited over the entire area and has since been eroded from the crest 
of the anticline and the present valley of Canadian River. 

In Taff’s opinion the Guertie sand was deposited by Canadian 
River. No inherent objection to this hypothesis is known, but since 





144 


STRUCTURE 


the Guertie sand occurs at scattered localities both north and south 
of the river it must be assumed that during the period of deposition 
the stream migrated and meandered back and forth through a con¬ 
siderable distance north and south. 

Springs are numerous along the base of the Guertie formation. 
Water which falls on the surface migrates downward through the 
unconsolidated strata of the formation. When the less porous beds 
of underlying formation are encountered the descent is arrested. 
The water then follows laterally ^through the basal gravels of the 
Guertie and emerges as springs at the lower levels along the out¬ 
crop. ;*! W. 

PLATE XXIII 



MASTODON TOOTH FOUND AT RED SPRINGS, SOUTHEAST OF 
$TEEDMAN, OKLA. 

*•# 

FOSSILS 

On the south line of sec. 10, T. 3 N., R. 5 E., one-fourth mile 
east of Sandy Creek, Mr. A. E. Brainerd found an elephant tusk em¬ 
bedded in gravels of the Guertie formation. This tusk was standing 
upright in the gravel which is taken to indicate the presence of ad¬ 
ditional parts of the skull in the beds below the surface. The great¬ 
est diameter of the exposed portion of the tusk was six inches and 
it is estimated to have had a complete length of more than six feet. 
At Red Springs, southeast of Steedmag in the western part of the 
Coalgate quadrangle, numerous bones of a Mastodon have been col¬ 
lected by people living in the vicinity. One of the teeth was photo¬ 
graphed and is figured in (Plate XXIII). This is a tooth of 







STRUCTURE 


145 


Mammut americanum and it is probable that the tusk found in the 
Stonewall quadrangle belonged to an animal of the same species. 

No Guertie sand is present in the vicinity of Red Springs, so 
that if it were established that the tooth from that locality had been 
deposited at the same time as the one found in the Guertie sand 
of the Stonewall quadrangle evidence would be available to further 
establish a stream origin for the Guertie. 

AGE 

The elephant tusk found by Mr. Brainerd suggests that the 
Guertie sand is of Pleistocene age. 

STRUCTURE 

The formation has an inclination toward the east which 
amounts to about 10 feet per mile. This probably represents the 
slope upon which the strata were deposited. 

ECONOMIC IMPORTANCE. 

The gravels from the basal part of the Guertie sand are quar¬ 
ried and used as road metal. The highway east of Ada is construc¬ 
ted of this material. 


RIVER SAND 

A thick deposit of white sand occurs in the valley of Canadian 
River and in the lower portions of its tributaries. This greatly 
resembles the weathered surface of the Guertie sand and where the 
two are adjacent the contact cannot be accurately drawn. In gen¬ 
eral, however, they may be distinguished by the following criterion: 
the Guertie sand occupies the hilltops while the river sand is con¬ 
fined to the valleys. 

The river sand is thought to be of recent origin. 

STRUCTURE 
GENERAL STATEMENT 

The structure of the formations exposed in the Stonewall quad¬ 
rangle can best be treated by dividing the area into two divisions. 
The general limits of these divisions are as follows: 

1. A northwestern area including all the strata above the 
Boggy formation, and 

2. A southeastern area including all the formations from the 
Boggy to the Arbuckle, inclusive. 

The former division covers about three-fourths and the latter 
about one-fourth of the quadrangle. 


146 


STRUCTURE 


NORTHWESTERN AREA 

GENERAL STRUCTURE 

The general structure of the northwestern area is monoclinal. 
The beds dip gently toward the northwest with an average inclina¬ 
tion of a little less than one degree. 

Since the Stonewall quadrangle lies along the northern flank 
of the Arbuckle Mountains it might be supposed that the strike of all 
the strata exposed there would conform to the general direction 
taken by the Arbuckle axis. This, however, is not the case. Ex¬ 
cept for a narrow zone along the Lawrence uplift, where the struc¬ 
ture of some of the formations is controlled by faulting, the strike 
of all the strata above the Boggy formation is almost at right angles 
to the mountain axis. This shows clearly that the regional move¬ 
ments, which resulted in the present general structure of the north¬ 
western part of the Stonewall quadrangle, were produced by dis¬ 
turbances that took place in some region outside of the Arbuckle 
Mountains. Since the dip of the strata in this northwestern area 
is toward the northwest the inference is that the region of disturb¬ 
ance was toward the southeast. In the latter direction, and rough¬ 
ly parallel with the strike of the strata now being considered, is the 
Choctaw fault. This fault conforms to the outline of the Ouachita 
uplift and was undoubtedly produced by movements occurring in 
that area. The trend of evidence thus available leads to the con¬ 
clusion that all or at least some of the movements which produced 
the Choctaw fault also controlled the dominant or normal structure 
of a large part of the Stonewall quadrangle. That there was pro¬ 
nounced faulting and some folding in the Arbuckle Mountains sub¬ 
sequent to the controlling disturbances of the Ouachita area is 
shown by the local conformity of the beds south of Ada to the fault 
which defines the northern limit of the Lawrence uplift. In a later 
paragraph the structure of the Lawrence uplift is discussed in detail. 

Superimposed upon the monoclinal slope of the formations, 
which outcrop in the northwestern part of the quadrangle, are a 
number of local structural features that are worthy of mention. Be¬ 
ginning at the north end of the area these are discussed in their or¬ 
der of geographic occurrence. 

SASAKWA ANTICLINE AND FAULT 
At the quarry one-fourth mile south of Sasakwa, the Sasakwa 
limestone, which is well exposed there, is folded into a narrow anti¬ 
cline, the axis of which trends toward the northeast. The east, or 
reverse, dip amounts to about 30 feet, but the fold does not close 
toward the northeast. Some years ago a well was drilled on this 
anticline to a reported depth of 1,200 feet. The log of the well was 
not secured, but on the basis of conclusions drawn in this report it is 


STRUCTURE 


147 


probable that the drill did not penetrate the horizons which yield 
the shallow oil at Allen. Because of the narrow width of the fold 
and the possibility of its diminishing downward, both as to width 
and relief, the probability of oil accumulations in horizons below 
those penetrated by the well is doubtful. If the fold was more 
pronounced there might be justification in sinking a deeper well to 
test the Allen sands, and in the event that these were unproductive 
to continue to the Hunton limestone, which is thought to occur here 
at a depth of about 3,400 feet. 

At the south end of the fold a normal fault of small throw 
trends in a direction slightly more east of north than does the axis 
of the anticline. 

ANTICLINE AT THE WESTERN EDGE OF T. 6 N., R. 7 E. 

Along the western edge of T. 6 N., R. 7 E. is a very narrow 
anticline which has a length of a little more than one mile. Near 
the center of the west line of section 19 the fold has a closure of 
nearly 25 feet, the east dip there being pronounced. The Belle 
City limestone is exposed in the area and affords an excellent key 
bed for use in mapping the structure. 

WEST END OF ALLEN ANTICLINE 

In sec. 31, T. 5 N., R. 8 E., is a western extension of the Allen 
anticline. The axis here is almost directly east-west. Anticlinal 
folding occurs along this axis as far west as section 32, south of 
Francis, and is thought to account for the oil production southeast 
of that town. This fold is parallel with the Lawrence uplift and al¬ 
though the two regions are separated by a distance of eight miles, 
it may be that the structure of each was influenced by the same set 
of movements. Faulting along the flanks of the Lawrence uplift 
suggests the possibility of a subsurface fault along the trend of the 
anticlinal axis west of Allen. With this hypothesis it might be as¬ 
sumed that the present observed folding of the latter area has re¬ 
sulted from later small movement along an already established fault 
line. 

The fold was nowhere observed to close toward the east. 
Several years ago a deep well was drilled on its crest east of the 
center of sec. 31, T. 5 N., R. 8 E. Small quantities of* oil are re¬ 
ported to have been yielded by several horizons, none of which were 
of commercial importance. 

It is thought that the Caney shale was encountered in this 
well, just below the Boggy formation, at a depth of 1,860 feet. If 
this supposition is correct the indication is that between the Caney 
and Boggy is an unconformity represented by the absence of the 
Wapanucka to Savanna formations, inclusive. This is in agree¬ 
ment with conditions observed on the Lawrence uplift. 


148 


STRUCTURE 


FOLD IN THE NORTHWEST CORNER OF T. 4 N., R. 8 E. 

Along the west side of sec. 6, T. 4 N., R. 8 E., is an anticlinal 
nose, the north-south axis of which is followed by a tributary of 
Muddy Boggy creek. The fold plunges toward the north and has 
a maximum structural relief of 50 feet. It opens rapidly toward the 
south and has no closing contours. 

In the northwest corner of section 5 is a small normal fault. 
The trend of this fault is northeast-southwest, but it is thought to 
die out before reaching the crest of the fold in section 6. 

BEEBE ANTICLINE 

North of Beebe is an anticline that opens toward the north¬ 
west. The axis of this fold extends from the southeastern part of 
sec. 32, T. 4 N., R. 5 E., to the same relative position in section 28 
of the same township. The maximum structural relief amounts to 
25 feet and at no place does the structure close toward the north. 

Wells drilled near the crest of the fold in the area north of 
Beebe encountered oil horizons in what is thought to be the Boggy 
formation at depths of 1,600 and 1,750 feet. Commercial quanti¬ 
ties of oil were yielded by the latter horizon. The Caney shale 
was penetrated at depths averaging 1,800 feet. 

A well drilled by the Nance syndicate near the north line of 
sec. 4, T. 4 N., R. 5 E., encountered Hunton limestone at a depth of 
2,305 feet. The identification of this limestone was determined 
from fossils 93 secured when the well was shot. The Hunton lime¬ 
stone was penetrated for a depth of 107 feet and when shot started 
flowing oil at the rate of about 100 barrels per day. 

The Beebe anticline is on the northeastern flank of the much 
larger Center anticline that is discussed in a later paragraph. 

FOLD SOUTHEAST OF MAXWELL 

A little more than one mile southeast of Maxwell is a 
broad anticlinal nose or terrace that opens rapidly toward the east. 
The axis of this fold extends from a point about one-half mile be¬ 
yond the western edge of the township eastward along the south 
line of sec. 18, T. 5 N., R. 5 E., and possibly continues as far as the 
juncture of this line with Canadian River. 

FOLD WEST OF OAKMAN 

A little more than a mile west of Oakman is a northwestward 
plunging anticline that in the northwest quarter of section 11 , T. 
4 N., R. 6 E., has a probable closure of nearly 10 feet. The struc¬ 
tural relief of the nosing portion of the fold is nearly 100 feet. The 
axis trends northwest-southeast and if projected in the former di- 


93 See page 3 7. 



STRUCTURE 


149 


rection would cut the down drop fault block that occurs in the 
region northeast of Byng. 

FAULT BLOCK NORTHEAST OF BYNG 

Approximately one mile northeast of Byng is a down- 
drop fault block. The trend of the block is northwest-southeast 
and the throw of the limiting faults is about 30 feet. The faults 
apparently die out both toward the east and west, but in the for¬ 
mer direction their continuation is marked by a downward flexing 
of the strata which results in the synclinal fold along the north side 
of the Oakman anticline. 

STRUCTURE OF THE ADA GAS FIELD 

Local folding is present in the Ada gas field and apparently 
controls the gas accumulation there. In the southeastern part of 
section 8, and the northeastern part of sec. 17, T. 4 N., R. 6 E., is 
a small dome with a closure of a little more than 20 feet. The axis 
of this fold is northeast-southwest. A structural contour map drawn 
on the surface of the Hunton limestone (See Plate IV) shows a 
northeastward projecting nose of the older formations beneath the 
surface of this area. 

It is thought that the gas derived from this field comes from 
sands in the Boggy formation. 

CENTER ANTICLINE 

West of the town of Center is the crest of a large anticlinal 
uplift, the axis of which extends from the bend in Spring Creek, in 
the south central part of T. 5 N.,R. 4 E., southeastward to the vicin¬ 
ity of Pickett. The width of the area effected by the fold is about 
five miles. 

From the areal map it is obvious that this broad arch is in 
close alignment with the axis of that portion of the Arbuckle 
Mountains which extends northwestward into the Stonewall quad¬ 
rangle. When it is considered that in relation to the area farther 
east, strata older than the Pennsylvanian have been encountered 
at comparatively shallow depths by wells drilled on the Center up¬ 
lift this alignment strongly suggests that, beneath the fold, there is 
a subsurface projection of the Arbuckle Mountains. The eastward 
dip of surface formations on the Center anticline may be best ob¬ 
served in the northwest part of section 11 and in the western por¬ 
tions of secs. 24 and 2 5, T. 4 N., R. 4 E. The eastern limit of the 
anticline is marked by a rather broad syncline, the axis of which 
follows a general southeasterly or parallel course from a point about 
two miles southwest of Maxwell, to the east of the town of Center 
and into the northeast corner of T. 3 N., R. 5 E. 

Several miles northeast of Stratford is a projection of the 


150 


STRUCTURE 


Center anticline that tends more toward the west than does the 
axis of the main uplift. The position of this minor fold supports 
the supposition that the inlier of limestone, exposed on the east line 
of sec. 2, T. 4 N., R. 3 E., is to be correlated with the upper part 
of the Hart limestone member of the Stratford formation. 

SYNCLINE SOUTH OF VANOSS 

South of Vanoss is a westward plunging syncline the 
axis of which extends from the east central part of sec. 1, T. 3 N., 
R. 4 E., southwestward into the northern part of section 9 of the 
same township. The maximum structural relief is about 70 feet. 

STEEP-DIP ZONE IN T. 3 N., R. 5 E. 

A belt of steeply-dipping strata extends in a northeast-south- 
westerly direction through the central part of T. 3 N., R. 5 E. The 
dip of these beds is toward the northwest. Upon first investigation 
it was thought that faulting was present along this zone, but further 
work failed to substantiate this supposition. It is thought probable 
that the unusually steep dip has resulted from movements that have 
taken place along a subsurface fault that was probably established 
in late Wewoka time. 


SOUTHEASTERN AREA 

GENERAL STRUCTURE 

In the southeastern portion of the Stonewall quadrangle the nor¬ 
mal dip of the strata, below the top of the Boggy formation, is 
northeastward; almost at right angles to the dip of the higher for¬ 
mations. The structure of the Boggy outcrop northeast of Law¬ 
rence, of some of the Pennsylvanian strata in the Franks graben, 
and of the portions of Arbuckle and Simpson formations along the 
western edge of the area is not in accord with this normal or gen¬ 
eral dip. 

For the sake of further convenience the area may be subdivid¬ 
ed into three smaller portions which will be discussed under the 
headings: Lawrence uplift, Franks graben, and the Arbuckle Mount¬ 
ains proper. 

LAWRENCE UPLIFT 

This uplift takes its name after the town of Lawrence which is 
located in the west central portion of the area. Eastward from 
Lawrence the uplift extends beyond the limit of the Stonewall quad¬ 
rangle and is thought to have a connection with the Savanna anti¬ 
cline of the CcaJgate quadrangle. The width of the uplift north 
and south is about six miles and its limits are defined by faults. The 
faults are normal and of the scissors type with their greatest throw 
near the western end of the uplift. 


STRUCTURE 


151 


The movement of the Lawrence block has been upward be¬ 
tween these limiting faults so that in reality it constitutes an east¬ 
ward plunging horst. 

AHLOSA FAULT 94 

At its western end the fault along the northern side of the up¬ 
lift has a throw of nearly 2,000 feet. The amount of movement 
decreases rather rapidly toward the east and in the northern part of 
T. 3 N., R. 7 E., the main fault apparently merges into a zone of 
small faults, and with these then dies out near the eastern edge of 
the quadrangle. In the region south of Ada all strata to near the 
top of the Wewoka formation are cut by the fault; and later beds, 
including those of the Francis, are sharply flexed and, in local 
areas, slightly faulted along a line representing its probable subsur¬ 
face trend westward. 


STONEWALL FAULT 95 

The fault on the south side of the uplift marks the northern 
boundary of the Franks graben. At the eastern edge of the quad¬ 
rangle beds at the base of the Boggy section, on the north side of 
the fault, are in contact with upper beds of that formation to the 
south. In this locality, therefore, the amount of throw that has 
been developed since the beginning of Boggy time appears to be 
only slightly less than the thickness of the formation or about 1,000 
feet. The phrase “appears to be” is used advisedly; for although 
there undoubtedly has teen some post-Boggy movement along the 
fault, as is indicated by such phenomena as drag and sudden change 
of strike, the conditions outlined are subject to another interpreta¬ 
tion which requires only sufficient faulting to explain the change of 
strike and drag observed. If the beds at the “base of the Boggy” 
on the north side of the Stonewall fault, although resting upon 
Wapanucka limestone and Caney shale, are not basal Boggy beds, 
but strata near the center of the formation and if the strata at the top 
of the section south of the fault are also of the middle part of the 
formation the obvious explanation would te that in early Boggy 
time the Lawrence uplift was above sea level and subject to erosion 
while the lower part of the formation was being deposited to the 
south. Then, when the uplifted area became peneplaned near mid¬ 
dle Boggy time, the sea might have spread over it so that through 
the remainder of Boggy time deposition would have been uniform 
over the region both north and south of the fault. This explana- 

94 The name is after Ahlosa store in sec. 24, T. 3 N., R. 6 E., about one mile 
south of the fault. 

95 The name is after the town of Stonewall that is located at the eastern 
edge of the quadrangle and just south of the fault. 



152 


STRUCTURE 


tion is less favored by the writer than the first one suggested, but 
has in its favor the fact that it requires a maximum thickness for 
the Boggy of about 2,400 feet which is near the thickness given the 
formation in the Coalgate folio. 

Preferment of the first interpretation, involving a total Boggy 
section of only 1,200 feet and post-Boggy displacement along the 
Stonewall fault of about 1,000 feet, is based on previously stated 
field observations that may be summarized as follows: 

1. The Ahlosa fault on the north side of the uplift is obvious. 

2. The Ahlosa fault cuts formations as high as the Wewoka and was 
therefore produced, or at least rejuvenated, in post-Boggy time. 

3. At the western end the Ahlosa fault has a throw of nearly 2,000 
feet. The throw gradually diminishes toward the east. 

4. The normal dip of formations exposed on the Lawrence uplift is 
toward the northeast. 

5. There is physical evidence of post-Boggy movement along the 
Stonewall fault. 

Unless it is assumed that there was at least as much post-Boggy 
movement along the Stonewall fault as along the Ahlosa fault, it is 
exceedingly difficult to explain the normal northeastward dip of the 
strata on the Lawrence uplift. 

Westward from the Wapanucka-Boggy contact lower and low¬ 
er strata, on the north side of the Stonewall fault, are in contact 
with Boggy strata of the Franks graben. The normal interval be¬ 
tween the Wapanucka and Boggy formations is probably between 
3,500 and 4,000 feet. This full section is thought to be present in 
the eastern end of the Franks graben. From these data it is con¬ 
cluded that, since the throw of post-Boggy faulting near Stonewall 
is not more than about 1,000 feet, the Stonewall fault must have 
been established in pre-Boggy time and that at some time before 
the Boggy was deposited the fault must have developed a throw of 
at least 2,500 feet. The post-Boggy movement was along this 
previously established fault line. 

MINOR FOLDING 

As previously stated, most of the strata exposed on top of the 
Lawrence uplift dip toward the northeast. Due to the combination 
of the normal northeastward dip of the area and the sharp down¬ 
ward drag of the strata along the north side of the Stonewall fault 
a narrow anticline is formed that extends along almost the entire 
length of the uplift. About one mile north of Frisco the down¬ 
ward drag to the north of the fault amounts to about 70 feet. A 
west dip of almost this same amount is also present on the anticline 


STRUCTURE 


153 


here. The combination of this west dip, the southward fault drag 
and the normal northeastward dip has resulted in a rather large 
dome. The Hunton formations which carry oil at Beebe and Maud 
are here probably not more than 800 feet below the surface. In a 
creek bed in the northern part of sec. 29, T. 3 N., R. 6 E., limestones 
in the Hunton terrane show considerable quantities of asphalt. With 
the Hunton formations as a prospective oil horizon, therefore, a 
drilling test of the Frisco dome is advisable. This dome lies in the 
southern part of section 4 and the northern part of sec. 9, T. 2 N., 
R. 7 E. Additional local folding on the Lawrence uplift is shown 
by a small anticline in the western part of sec. 15, T. 3 N., R. 6 E 
(an inlier of Woodford is here surrounded by Caney shale) and 
by the rather complicated folding of the narrow exposure of Boggy 
strata that occurs along the escarpment northeast of Lawrence. In 
the latter area beds belonging to the top of the Wewoka formation 
rest uncomformably on the folded Boggy strata. 

FRANKS GRABEN 

The Franks graben is triangular in shape, converging toward 
the west. The general structure of the strata within it consists of 
two sharp drag synclines, along the limiting east-west faults, and 
between these, of a broad westward plunging anticlinal fold. The 
anticline opens toward the east so that at the eastern edge of the 
quadrangle the normal dip is almost directly north. The fault along 
the northern side of the graben divides it from the Lawrence uplift. 
The fault at the south side is plainly visible about one-fourth mile 
south of Franks. It is here marked by an east-west escarpment that 
extends through the central portions or secs. 34, 35, and 36, T. 2 N., 
R. 6 E., and into sec. 31, T. 2 N., R. 7 E. In the latter section it 
apparently dies out. At the western end of the Franks graben this 
southern fault, if present-,-is overlapped by Holdenville strata. The 
narrow syncline that occupies the region just north of the fault, in 
the vicinity of Franks, is also not to be observed in the western part 
of the graben and, like the fault, may there be covered by overlap¬ 
ping Holdenville beds. This is also the case with the syncline on 
the north side of the graben. 

Although the fault which marks the southern side of the 
graben dies out southeast of Franks the narrow syncline along its 
northern side continues southeastward and may be traced to near 
the eastern edge of the quadrangle. 

The anticline which occupies the central part of the graben 
cannot be traced much farther west than the town of Franks. Along 
the north side of the graben, almost directly north of Franks, there 
is a rather large divergence in the structural contours. It is thought 
that this line of divergence marks the position at which the Boggy 


L54 


STRUCTURE 


formation passes beneath the overlapping strata of the late Wewo- 
ka and subsequent formations. If this is the case, the westward dis¬ 
appearance of the anticline near the center of the graben may be 
accounted for by assuming that it also is covered by overlapping 
strata that were deposited subsequent to the anticlinal folding. 

West of Franks in the northwest quarter of sec. 34, T. 2 N., 
R. 6 E., the Hunton formations are cut by several block faults. These 
were described in detail by Reeds. 96 An item of importance, how¬ 
ever, which was not mentioned by Reeds is that the block faults 
here also cut the Pennsylvanian (Holdenville) strata. (See Plate 
XXVI). This shows that the movement took place after the 
Holdenville formation had been deposited 

PLATE XXVI 



OFFSET FAULT IN HOLDENVILLE FORMATION. 

Location northeast quarter, sec. 34, T. 2 N., R. 6 E., just north of the Hunton 
fault blocks described by Reeds. Picture taken looking west. 

To the west of Franks, beyond the points where the central 
anticline and the bordering synclines of the graben lose their iden¬ 
tity, by passing beneath overlapping beds, the strata around the V- 
shape border of the area dip inward and produce a general synclinal 
structure. Within this small basin-like area is some local folding. 

For further sake of convenience, the structure of the strata 
which outcrop between the Franks graben proper and the edge of 
the Arbuckle Mountains, may be discussed with this area. The 
normal dip of these beds is northeast. In the detailed discussion 
of the stratigraphy of this area it has been assumed that the north¬ 
westward disappearance of the lower Pennsylvanian strata, be- 

96 Reeds, C. A., Okla. Geol. Survey, Bull. No. 3, p. 50, 1910. 




STRUCTURE 


155 


tween the eastern edge of the quadrangle and the town of Franks, 
is the result of overlap by the Hartshorne and McAlester formation, 
particularly the latter. It is here desired to point out the fact how¬ 
ever, that this disappearance of formations (Wapanucka to Harts¬ 
horne, inclusive) might also be plausibly explained by the assump¬ 
tion of a fault in the area. At the western edge of the Coalgate 
quadrangle Taff 97 shows a dotted fault along the northern edge of 
the Wapanucka outcrop. If this fault were assumed to have its 
uplift to the south, as would be expected since the mountains are 
in that direction, and if the trace of the fault were assumed to angle 
slightly toward the mountains, across the strike of the beds, its opera¬ 
tion, connected with subsequent erosion, would account for all the 
disappearance of beds which has been explained by overlap. Evi¬ 
dence was not secured with which to either prove or disprove the 
presence of such a fault. In the creek bed in sec. 1, T. 1 N., R. 6 E., 
however, a bed in the McAlester shale was observed resting upon 
the Caney. (Plate IX). At this point the contact was marked by a 
conglomerate which carried Pennsylvanian fossils and the evidence 
was clear that no fault was there present. This condition estab¬ 
lishes the fact that if such a fault exists it is of pre-McAlester age. 
Other evidence bearing on the problem is that no definite indica¬ 
tions of faulting were observed. The fact that overlap exists is 
clear and since such overlap easily accounts for the disappearance 
of the Wapanucka, Atoka, and Hartshorne formations near Franks, 
it is considered by far the more plausible explanation. 

STRUCTURE OF THE ARBUCKLE MOUNTAINS PROPER 

The structure of that portion of the Arbuckle Mountains proper 
which extends into the Stonewall quadrangle has been discussed in 
the treatment of the Arbuckle, Simpson, and Viola formations. Sum¬ 
marizing that discussion it may be said that the area constitutes a 
broad, northward-plunging, anticlinal projection from the main mass 
of the mountains farther south. Much of the bordering area is 
limited by faults, the downthrow sides of which are away from the 
central part of the uplift. 

At the eastern edge of the area are a number of small normal 
east-west faults. These are nearly parallel with the dip and re¬ 
semble each other in that the upthrow side of each is to the south. 

The northward projecting axis that lies between Roff and 
Lawrence is thought to have a general continuation beneath the 
Center anticline. 


97 U. S. Geol. Survey. Geol. Atlas Coalgate Folio, No. 74, 1901. 



156 


CORRELATION 


SUBSURFACE STRUCTURE 

In the northern and western portions of the Stonewall quad¬ 
rangle the surface and subsurface structure shows considerable vari¬ 
ation. This may best be appreciated by a comparison of the struc¬ 
tural map drawn on the surface of the Hunton terrane (Plate VII) 
and the map showing the present surface structure (Plate XXIV). 
The most striking difference shown by these maps is in the region 
north of the Lawrence uplift and east of Center anticline. The 
surface structure of this area is that of a northwestward sloping 
monocline while the subsurface structure of the Hunton limestone, 
and presumably that of all beds lower than the Wapanuka, is, in 
general, monoclinal to the northeast. 

The presence of a subsurface fault is indicated along the steep 
dip zone that extends in a northeast-southwesterly direction through 
the central part of T. 3 N., R. 5 E. 

The data used in making the structural map of the Hunton 
terrane is given in the dicussion of the formations that comprise that 
division. 


CORRELATION 

The correlations here suggested are based entirely upon faunal 
and floral evidence and were derived by comparing the average 
maximum range of all the fossils collected in the Stonewall quad¬ 
rangle with the average maximum range of similar species from 
adjoining areas. No profession is made as to the accuracy of the 
results. They are in close, but not strict accord with other cor¬ 
relations that have been suggested and are given merely as the best 
evidence available to the writer. Probably the greatest divergence 
from earlier correlations is presented by the Calvin and associated 
formations. S'iebenthal 98 considered the Calvin to be approximate¬ 
ly equivalent to the Fort Scott of Kansas and apparently has been 
followed in this belief by most geologists interested in the strati¬ 
graphy of eastern Oklahoma. Evidence for the correlation by 
Siebenthal, however, is inconclusive and with our present knowledge 
of the many unconformities and overlaps which occur in the Penn¬ 
sylvanian strata of eastern Oklahoma, it seems advisable to present 
the faunal correlations here determined. 

Wide divergence with earlier stratigraphic studies is also made 
as regards the position of the Pennsylvanian-Permian line. The 
contact between these two systems has previously been placed about 
20 miles to the west of the contact shown on the areal map of the 
present report. The evidence presented by the fossils, however, 
seems to justify the change here indicated. 


"Siebenthal, C. E. 



PLATE XXVII 


CORRELATION TABLE 

Of 

Mississippian, Pennsylvanian and Permian 

Nofer-Tneae cor re lotions ore bosecJ on average range g percent of Common species 


Stonewall Quadrangle 
Oklahoma 


north Central 
Texas 


Ka 


nsas 


missouri 


kilter Sand 

Quertie Sand 


Asher 


Konawa 


Stratford 

Una mealier'. 


Vanoss 


Ada 


Vamoosa 


~EeITe Z'fr 


Francis 


Seminole 


Holdenv/lle 


Permian 


Permian 


Putnam 


iTloran 


Pueblo 

Harpersuille 

Thrifty 


Qraham 


Wobaun%ee 


Wabaunsee 


5ha.\r/r>te 


QouS/a 5 


Lansing 


Shawnee. 


Douglas 


Lansi ns 


Wcwoka 


Wetumka 


Calvin 


Sen ora 


Stuart 

Thurman 


Boycjij 


Sai/anna 


Wit (Hester 


Hartshorne 


dtok a. 


Wapanucka. 


Caddo Creek 


Brad 


Kansas City 


Kansas City 


Upper Cane.y 
Lower Caneij 


Graford 


Palo Pinto 


marmaton 


THarmaton 


IThneral Wells 


Cherokee 


Cherokee 


Wills ap 


Srmthwick 


marble Falls 


-XSyeamore 


Upper Woodford 

Lower u/oodford 


Barnett 

? 



























































158 


WELL. LOGS 


In the discussions devoted to the individual formations the cor¬ 
relation of each is given. 


WELL LOGS 

A great deal of information regarding the conditions of the 
subsurface stratigraphy of the Stonewall quadrangle is made avail¬ 
able by a consideration of the records of deep wells drilled in the 
area. For this reason a list of what are considered the most im¬ 
portant well logs is here included. 


SB. Cor. see. 11, T. 2 N., R. 3 B. Garznn County, Oklahoma 
Golde'ine Petroleum Co. 

Ground elevation 1200 ft. 


1 

CHARACTER OF ROCK. | 

Thick- 1 
ness | 
1 T >"t | 

Depth 
| F-t 

CHARACTER OF ROCK. | 

1 

Thick¬ 

ness 

Feit 

Depth 

1 Feet 

Soil 

0 

10 

Lime 

2 

832 

Red rock 

20 

30 

Shale 

48 

880 

Shale 

295 

325 

Limp . 

2 

882 

Red rock 

5 

330 

Shale 

33 

915 

Shale 

1 5 

345 

Lime 

65 

980 

Red rock 

10 

355 

Sand with HoS 

18 

998 

Shale 

9 01 
15] 

445 

Limp. 

112 

1110 

Rad rock 

| 460 

Light gr;en shale_ 

10 

1120 

Lime 

90 
50] 
I 10 

550 

Limp 

70 

1190 

Shale 

600 

Sand 

25 

1215 

Lime 

I 610 

Lime 

215 

1430 

Shale 

40 

1 650 

Sa-'dy lime 

30 

1460 

Lime 

2 

652 

Broken lime 

30 

15 

I 1490 

Shale 

| 38 

690 

Limey said 

15 05 

Limp 

3 

693 

Lime 

15 

1520 

Shale 

| 22 

715 

Sandy limp 

200 

1720 

Lime 

1 10 

725 

Lime 

| 80 

1800 

? 

! 15 

740 

Sandy lime 

1 30 

1830 

Sand 

1 10 

750 

Lime 

1 42 

I 1872 

Shale 

| 10 

760 

Sa^dy lime 

8! 1880 

Sand 

1 50 

810 

Lime 

| 30 

1910 

Lime 

I 10 

820 

Sandy lime 

1 96 

2006 

S^ale . . 

1 10 

1 830 

! 



Correlation:—The recks encountered in this well from 760 feet to 
1,215 feet have been tentatively correlated as Simpson, and those from 1,215 
feet to 2,006 feet as a part of the Arbuckle. 


























































WELL LOGS 


159 


¥ 


Magnolia Petroleum Co. No. 1, SB, SW, NB, sec. 31, T. 5 N., R. 8 B. 
Pontotoc County, Oklahoma. 


Ground elevation, 940 feet. 


CHARACTER OP ROCK. 

Thick¬ 

ness 

Feet 

Depth 

Feet 

CHARACTER OF ROCK. | 

1 

Tn.ck- | 
nesj | 
Feet 

Depth 

I Feet 

Surface 

90 

90 

Blue slate | 

45 

1440 

Sand 

15 

105 

Sand 

2 5 

146 5 

Slate 

30 

135 

Black slate 


1 T U J 

\ 47 c 

Sand 

30 

160 

White slate 

l J 

oq 

1^/0 

1 5 0 7 

Slate 

20 

1 80 

Sandy shale 

j 

Q 

1 JU/ 

1 5 1 6 ' 

Sand (water) 

40 

220 

Blue slate 

J 

54 

1 J 1 

15 70 

Slate 

112 

332 

Sand (some gas)_ 

5 

1575 

Sand 

34 

366 

Water 

5 

15 80 

Slate 

214 

580 

Blue slate 

2 

1582 

Sand (show oil)_ 

32 

612 

Lime 

12 

1594 

Slate 

18 

630 

Sand 

7 

1601 

Sand 

50 

680 

Slate 

26 

1627 

Red rock (water)_ 

10 

690 

Sand (some gas)_ 

6 

1633 

Sand 

35 

725 

Blue slate 

4 

1637 

Slate 

80 

805 

White slate 

13 

1 650 

Sand (show oil)_ 

5 

810 

Blue slate 

40 

1690 

Slate (water) 

10 

820 

Lime 

5 

1695 

Lime 

5 

825 

Blue slate 

30 

1725 

Sand (water) 

10 

835 

Black slate 

20 

1745 

Blue slate 

15 

850 

Blue slate 

1 5 

1760 

Black slate 

100 

950 

Sand 

1 5 

1775 

BIup slate 

35 

985 

Blue slate 

20 

1 795 

Red rock 

24 

1009 

Sand 

15 

1810 

Slate 

23 

1032 

Black slate 

15 

1820 

White slate 

53 

1085 

Sand . 

10 

1830 

Sand 

9 

1094 

Red slate 

5 

1835 

Red rock 

6 

1100 

Blue slate 

20 

1855 

Slate 

25 

1125 

Sand - 

5 

1860 

Lime 

8 

1133 

Black slate 

30 

1890 

Pink slate 

12 

1145 

Blue slate 

60 

205 0 

Sand 

3 

1148 

Black slate 

60 

2110 

Lime 

7 

1155 

Blue slate 

70 

2180 

blue slate 

45 

1 200 

Black slate 

18 

2198 

Lime 

5 

1205 

Lime 

6 

2204 

Sand (water) 

10 

1215 

Blark slatp 

41 

2245 

Black slate 

25 

1240 

Blue slate 

60 

2305 

Blue slate 

15 

1255 

Black slate 

17 

2322 

Black slate 

25 

1280 

Sand 

18 

2340 

Sand 

6 

1286 

Blue slate 

55 

2395 

Shale 

14 

1300 

Black slate 

45 

2440 

Sand _ 

5 

1305 

Blue slate 

65 

2505 

Slate 

59 

1364 

Blue shale 

80 

2585 

Lime 

5 

1369 

(Hole full water at 



Blue slate 

21 

1390 

2 515) 



Brown slate 

5 

1395 


1 

1 


Correlation:—This log is important in indicating the unconformity be¬ 
neath the Boggy formation. The formations penetrated in this well from 
1,860 feet to 2,585 feet have been correlated as Caney and Woodford. 






























































































160 


WELL LOO 


Hoggard No. 1, sec. 4, T. 4 N., R. 5 R., Pontotoc County, Oklahoma 

Nance Syndicate. 


CHARACTER OF ROCK. 

Thick¬ 

ness 

Feet 

Depth 

Fe^t 

CHARACTER OF ROCK. 

| Thick- 

| ness 
| Feet 

1 

| Depth 
| Feet 

Surface tn clay 

4 

4 

Sandy shale 

45 

865 

Sand rock 

26 

30 

Blue shale 

15 

880 

Red bed 

72 

102 

Red rock 

25 

905 

Sand rock 

20 

122 

Water sand 

30 

935 

Blue shale 

8 

130 

Blue clay 

35 

970 

Red rock 

22 

1 52 

Red rock.. 

30 

1000 

Brown shale 

18 

1 70 

Blue shale 

20 

1020 

Water travel 

1 5 

185 

Water sand 

20 

1040 

Red rock 

10 

195 

Blue clay 

20 

1060 

White shale 

25 

220 

Black shale 

50 

1110 

Brown shale 

10 

230 

Linie (hard) 

12 

1122 

White shale 

15 

245 

Blue clay 

15 

1137 

Soft sand 

7 

252 

Black shale 

30 

1167 

White shale 

48 

300 

Sandy shale ... 

8 

1175 

Red rock 

20 

320 

Red rnck 

15 

1190 

Lime 

10 

330 

Black shale 

35 

1225 

Red rock 

20 

3 50 

Water sand 

25 

1250 

Blue clay 

10 

360 

Sand lime 

25 

1275 

Red rock 

20 

380 

Black shale 

35 

1310 

I .i m e 

10 

390 

Lime shell . 

10 

1320 

Red rock 

25 

415 

Blue clay _ 

15 

1335 

Limestone 

7 

422 

Black shale 

39 

1374 

Red rock 

8 

430 

Blue clay 

16 

1390 

Lime shell 

2 

432 

Water sand 

20 

1410 

Red rock 

12 

444 

Blue clay 

25 

1435 

Oil sand 

30 

474 

Blue sandy shale_ 

45 

1480 

Red rock 

36 

510 

Black shale 

70 

1550 

Lime shell 

6 

516 

Sandy shale 

10 

1560 

Red rock 

34 

550 

Oil sand 

20 

1580 

Shell lime 

5 

555 

Oil sand (good) 



Red rock 

20 

575 

(Showing of oil)_ 

20 

1600 

Blue clay 

25 

600 

Black shale 

15 

1615 

Red rock 

20 

620 

Sandy lime 

25 

1640 

Lime shell 

5 

625 

Black shale 

70 

1710 

Blue clay 

10 

635 

Hard Shell 

2 

1712 

Water sand 

25 

660 

Black shale 

63 

1775 

Red rock 

45 

705 

Sand (oi 1 ' 

3 

1778 

Water sand ; 

2.5 

730 

Black shale 

142 

1920 

Red rock 

30 

760 

Sand (oiH 

10 

1930 

Water sand 

15 

775 

Brown and black shale 

375 

2305 

Blue shale 

1 5 

790 

White lime 

107 

2412 

Lime 

5 

795 

Still in lime 



Blue shale 

25 

820 





Correlation:—A limestone encountered at 2,305 feet was penetrated to 
a depth of 107 feet and gave an initial production of 125 barrels. Fragments 
of fossils obtained from this limestone were identified by Professor J. J. 
Galloway of Columbia University. From the evidence afforded he stated, that 
the formation was of Niagaran age probably the equivalent of the Henryhouse 
shale of the lower Hunton. 





























































































WELL LOGS 


161 


IVell —150 feet from JSi. line and 150 feet from B. line, sec. 
14, T. 5 N., R. 4 B., Pontotoc County, Oklahoma. 
Transcontinental Oil Co. 


CHARACTER OF ROCK. 

Thick¬ 
ness 
| Feet 

Depth 

| Feet 

CHARACTER OF ROCK. ^ 

Thick- | 
ness 

1 Feet 

| Depth 
Feet 

Clay 

27 

27 

Lime and granite 



Lime, hard, white_ 

3 

30 

(granite-pieces of 



Shale, red, soft_ 

20 

50 

feldspar in the lime) 

3 

925 

Shale, blue 

17 

67 

Shale, brown, soft_ 

13 

938 

Sandy shale, red_ 

18 

85 

Lime 

2 

940 

Sandy shale, red_ 

12 

97 

Shale, Brown 

4 

944 

Mud, blue 

13 

1 10 

Shale, blue 

24 

968 

Shale, red 

47 

157 

Water sand 

8 

976 

Water sand, white not 



Shale, brown, soft __ 

5 

981 

enough for drilling 

13 

170 

Lime, white, hard __ 

4 

985 

Mud, blue 

5 

175 

Shale, brown 

5 

990 

Shale, red 

SO 

225 

Water sand, white_ 

6 

996 

Shale, gray 

11 

236 

Shale, brown 

1 7 

1013 

Shale, red caving_ 

74 

310 

Water sand 

12 

1025 

Shale, gray 

65 

375 

Shale, brown 

25 

1050 

Sand, little water_ 

5 

380 

Water sand (hole full 

Sandy lime 

10 

390 

of water 

15 

1065 

Water sand, white, 6 



Lime, hard 

l 

1066 

bailers per hour __ 

12 

402 

Water sand 

9 

1075 

Shale, blue 

5 

407 

Shale, red, soft_ 

49 

1124 

Shale, red 

25 

432 

Water sand, white_ 

8 

1132 

Water sand 

13 

445 

Lime, hard - 

2 

1134 

Sandy lime 

16 

461 

Shale, brown 

26 

1160 

Shale, blue 

22 

483 

Shale, blue 

95 

1255 

Sandy lime,white,hard 

12 

495 

Shale, brown 

10 

1265 

Shale, red 

1 40 

635 

Shale, blue 

10 

1275 

Water sand, white — 

25 

660 

Water sand, white __ 

20 

1295 

Lime, white, hard __ 

5 

665 

Lime 

1 5 

1310 

Sand 

1 2 

677 

Shale, blue 

22 

1332 

Shale, blue 

43 

720 

Shale, brown 

2 

1334 

Lime, white hard_ 

12 

732 

Lime, white 

10 

1344 

Shale, blue, soft_ 

23 

755 

Shale, blue 

68 

1412 

Shale, red 

2 

757 

Shale, brown 

18 

1430 

Slate, black 

8 

765 

Shale, blue 

25 

1455 

Water sand, white, __ 

10 

775 

Sand, dry 

10 

1465 

Shale, blue 

13 

788 

Shale, blue, soft- 

15 

1480 

Shale, ypi 1 

6 

794 

Lime 

5 

1485 

Sand, white 

6 

800 

Shale, blue, soft- 

20 

1505 

Shale, blue 

16 

816 

Shale, black 

10 

1515 

Shale, yellow 

8 

824 

Shale, bine . 

85 

1600 

Sand 

10 

834 

Shale, black 

5 

1605 

Red bed 

20 

854 

Shale, blue 

21 

1626 

Sand 

12 

866 

Sand, show oil 

2 

1628 

Mud, blue 

6 

872 

Shale pink 

2 

1630 

Lime 

15 

887 

Shale, blue 

72 

1702 

Shale, soft, brown __ 

16 

903 

Sand, white (gas) — 

20 

1722 

Lime, and granite(this 



Shale, blue 

98 

1820 

reported granite was 



Red bed 

5 

1825 

probably pieces of 



Shale, brown 

15 

1840 

feldspar in the lime) 

17 

920 

Shale, black 

25 

1865 

Shale, brown 

2 

922 

Shale, blue 

35 

1900 


















































































162 


WELL LOGS 


Well —150 feet from N . line and 150 feet from B. line, sec. 
14, T. 5 N., R. 4 R., Pontotoc County, Oklahoma. 


Transcontinental Oil Co.—(Continued). 


CHARACTER OF ROCK. | 

Thick¬ 
ness | 
| Feet 

Depth 
| Feet 

CHARACTER OF ROCK, j 

| Thick¬ 

ness | 
| Feet 

! Depth 

| Feet 

Shale, black 

5o 

1950 

Shale, blue, soft_ 

70 

2340 

Shale, white, sandy - 

1 1 

1961 

Shale, black 

42 

2382 

Lime hard 

4 

1965 

Shale, gray 

15 

2397 

Shale, blue, soft- 

27 

1992 

Shale, gray 

73 

2470 

Lime 

5 

1997 

Shale, blue, soft- 

20 

2490 

Shale, blue, soft_ 

63 

2060 

Shale, and lime shells 

10 

2500 

Lime, hard 

10 

2070 

Shale, black 

80 

2580 

Shale, blue, soft_ 

15 

2085 

Shale, brown 

95 

2675 

Lime 

5 

2090 

Shale, and lime shells 



Shale, blue, soft- 

52 

2142 

Hunton Ls. 

10 

2685 

Lime 

16 

2158 

Lime, white, hard 

95 

2780 

Shale, blue 

92 

2250 

Slatp, snff 

90 

2870 

Lime, brown 

2 

2252 

SH11 drilling 



Sand, little water- 

18 

2270 





Correlation:—This well encountered a lime at 2,660 feet. This lime 
differed from that in the Nance well in that it was only 50 feet thick and 
made but a very small showing of oil. No fossils were secured from it, but 
the similarity of the logs of the two wells and their proximity strongly in¬ 
dicate that the two occurrences are part of the same formation. 


Sec. 24, T. 2 N., R. 4 B. In the City of Roff, 
Pontotoc County, Oklahoma. 


i 

CHARACTER OF ROCK. 

Thick- 
| ness 

I Feet 

Depth 

Feet 

i 

CHARACTER OF ROCK. | 
1 

Thick- | 
ness 
Feet ! 

| Depth 
| Feet 

Soil 

20 

20 

Limp . 

20 

840 

Lime, hard 

100 

120 

Sand, watpr 

40 

880 

Sand, show of oil_ 

20 

140 

Lime and shale_ 

60 

940 

Shale, slaty 

105 

255 

Sand, water 

60 

1000 

Lime 

5 

260 

Lime 

40 

1040 

Sand 

200 

460 

Lime very hard_ 

62 

1 102 

Shale, white and blue 

360 

820 





Correlation:—The rocks encountered in this well from 20 feet to 1,000 
feet have been correlated as the Simpsion formation, and those from 1,000 
feeet to 1,102 feet as Arbuckle limestone. 











































WELL LOGS 


163 


NW. J4i» sec. 28, T. 3 N., R. 7 B., Pontotoc County, Oklahoma 
Chas. Owen Co. No. 1 
Ground elevation, 782. 


CHARACTER OF ROCK. | 

Thick- | 
ness j 
1 Feet 

Depth 

I Feet 

1 

CHARACTER OF ROCK. | 

1 

Thick- | 
ness | 
Feet 

( Depth 
| Feet 

Surface 

28| 

28 

Black shelly shale __! 

3 51 

305 

Lime 

4 0 1 

68 

Black mud shale_ j 

445 

750 

Red mud slate 

92] 

160 

Brown mud and shale I 

1 5 o| 

900 

Sand (Fresh water) 

110 

270 

Hard lime(Salt water) j 

2 7 0 1 

| 1430 


Correlation:—In this log the rocks from 28 feet to 900 feet are cor¬ 
related as Caney and Woodford, and the thick, hard lime as the Hunton. 

Note:—Figures for individual thicknesses are in error, but could not be 
checked. Total thicknesses of formations are approximately correct. 


W. V. Cook, Well No. 1, NB. cor., NW%, sec NB% } sec. 20, 

T. 5 N., R. 4 B. 


Doan Oil Co. 


CHARACTER OF ROCK. 

Thick¬ 

ness 

Feet 

Depth 

Feet 

CHARACTER OF ROCK. 

1 

1 

I 

Thick- 1 

ness | 
Feet [ 

Depth 

Feet 

Sand and red mud __ 

3 5 

| 35 

Lime shells 

-1 

5 | 

1031 

Coarse gravel-water _ 

20 

1 55 

Gray shale 

-1 

16| 

1047 

Red rock 

25 

80 

Blue shale 

| 

5] 

1052 

Coarse gravel 

10 

90 

Li me 

| 

3| 

1055 

Sand rock 

10 

100 

Sand (Water sand at 

! 

1 


Red rock 

140 

240 

1060 feet) 

1 

1 o] 

1065 

Lime shells 

15 

255 

Red rock 

1 

lol 

1075 

Red rock 

70 

325 

Sand 

I 

111 

1086 

Brown shale 

62 

394 

Li me 

I 

4| 

1090 

Lime 

5 

399 

Red rock 

I 

3| 

1093 

Brown shale 

11 

410 

Lime 

1 

51 

1098 

Sand rock 

15 

425 

Red rock 

1 

59| 

1157 

Brown shale 

15 

440 

Sand 

I 

8| 

1165 

Red rock 

45 

485 

Blue Slate 

1 

251 

1190 

1 \ O 1 V- — — — — — 

Redi sand rock 

15 

500 

Red rock 

1 

151 

1205 

Red rock 

65 

565 

Lime shells and shale 

1 

71 

1212 

Sand (Water at 580') 

40 

605 

Blue slate 

1 

13] 

1225 

Red rock 

75 

680 

Blue shale 

J 

ioi 

1235 

1\LU i wvrv —- — —-- — — 

Sand ('Water') 

12 

692 

Blue slate 

J 

1 oj 

1245 

oaJiu \ ▼» ttici / —- 

Red rock 

46 

738 

Sand 

! 

51 

1250 

1\CU 1 - 

Time shells 

12 

750 

Blue slate 

I 

ioi 

1260 

Red rock 

40 

790 

Sand 

f 

51 

1265 

1\ C U 1 UIK-- 

Red rock-shale 

25 

815 

Blue slate 

J 

51 

1270 

1\ C U 1 ut Jv oiitU v-- 

Red rock 

1 60 

975 

Sand 

_! 

ioi 

1280 

I\CU 1 ULfk.-—- 

Time 

15 

990 

Blue shale 

_! 

151 

1295 

Red rock 

13 

1003 

Sandy lime 

1 

151 

1310 

1\ t U 1 Ot/lV-- 

Lime and shale - 

6 

1009 L 

Red rock 

J 

ioi 

1320 

White shale 

5 

1014 | 

Sand 

I 

ioi 

1330 

VV 1111^ 011 — —-— 

Sn nd shell 

l 

1015 

Sandy lime 

! 

23! 

1353 

Oduu on tn -— — 

Red rock 

11 

1026 1 


i 

1 













































































164 


WELL LOGS 


W. V. Cook, Well No. 1, NB. cor., NW'A, NEfa sec. 20, 
T. 5 N., R. 4 B. 

Doan Oil Co.—(Continued). 


CHARACTER OF ROCK. 

Thick¬ 

ness 

1 ^eet 

Depth 

Feet 

CHARACTER OF ROCK. 

| Thick- 
| ness 

1 Feet 

f Depth 
! Fept 

Sand 

27 

1380 

Blue slate and lime 



Lime 

5 

1385 

shells 

3 

1868 

Blue shale 

5 

1390 

Black shale 

22 

1890 

Lime and sand shells 



Light blue shale_ 

25 

1915 

(small oil show) _ 

23 

1413 

Blue shale 

27 

1942 

Red rock 

12 

1425 

Black shale 

20 

1962 

Sand 

5 

1430 

Lime shell 

3 

1965 

Lime 

23 

1453 

Blue shale 

1 7 

1982 

Red rock 

11 

1464 

Lime-shells 

3 

1985 

Blue slate 

22 

1486 

Blue shale 

18 

2003 

Brown shale and lime 



Black shale 

2 

2005 

shells 

14 

1500 

Black slate 

4 

2009 

Blue shale 

12 

1 5 12 

Blue shale . 

6 

2015 

Red rock 

3 

1515 

Black shale . 

10 

2025 

Sand 

10 

1525 

Blue shale 

10 

2035 

Slate 

15 

1 540 

Black shale 

10 

2045 

Blue slate 

5 

1545 

Blue shale 

5 

205 0 

Rlne slate 

10 

1555 

Sandy lime 

10 

2060 

Blue shale 

15 

1570 

Black shale 

65 

2125 

Blue slate 

5 

1575 

Blue slate 

10 

2135 

Blue shale 

11 

1586 

White slate 

10 

2145 

Blue slate 

6 

1592 

Blue slate 

5 

21 50 

Blue shale 

3 

1595 

Lime 

30 

2180 

Rlne slate 

10 

1605 

White slate 

10 

2190 

Blue shale 

10 

1615 

White slate 

10 

2200 

Red rock 

1 7 

1632 

Black slate 

5 

2205 

Blue slate 

3 

1635 

Blue slate 

5 

2210 

Sand 

5 

1640 

Black slate 

10 

2220 

Blue shale 

8 

1648 

Blue slate 

8 

2228 

Sand 

12 

1660 

Black slate 

10 

2238 

Rlne slate 

23 

1683 

Black shale 

7 

2245 

Red rock 

7 

1690 

Black slate 

15 

2260 

Blue shale 

20 

1 710 

Sand—dry 

20 

2280 

Lime 

15 

1725 

White slate 

15 

2295 

Blue shale 

7 

1732 

Blue slate 

25 

2320 

Blue slate 

6 

1738 

Sand water 

5 

2325 

Blue shale and sand 



Black slate and lime 



shells 

12 

1750 

shells 

10 

2335 

Sand 

15 

1765 

Sand—water 

10 

2345 

Blue slate 

10 

1775 

Lime, hard 

5 

2350 

Blue shale 

6 

1781 

Lime 

5 

2355 

Lime 

10 

1791 

Black slate 

5 

2360 

Sand—water jl 

24 

1815 

Black slate 

100 

2460 

Blue shale 

5 

1 820 

Blue slate 

25 

2485 

Blue shale and lime 



Black slate 

15 

2500 

shells 

7 

1827 

Sandy lime 

5 

2505 

Blue slate 

16 

1843 

Sand and lime 

10 

2515 

Lime shells 

7 

1850 

Sand 

10 

2525 

Lime 

5 

1855 

Sandy lime, hard_ 

5 

2530 

Sand 

2 

1857 

Lime, hard 

10 

2540 

Blue slate 

8 

1865 

Lime, sand, and shale 










































































































WELL LOGS 


165 


W. V. Cook, Well No. 1, NB. cor., NWy 4 , NE 1 /^ sec. 20, 

T. 5, R. 4 E. 

Doan Oil Co.—(Continued). 


1 

CHARACTER OF ROCK. 

Thick- ] 
ness | 
1 Feet 

Depth 

Feet 

l 

CHARACTER OF ROCK. 

Thick- l 

| ness 
| Feet 

Depth 

Feet 

(broken formation) 

10 

2550 

White shale 

10 

2655 

Lime and shale 

10 

2560 

White slate 

10 

2665 

Shale—black 

1 0 

2570 

White shale 

10 

2675 

Shale—soft 

5 

25 75 

White slate 

10 

2685 

Sh alp—white 

5 

2580 

White shale 

40 

2725 

Lime 

5 

2585 

Blue shale 

5 

2730 

Lime hard 

5 

2590 

Black shale 

5 

2735 

Lime hard 

15 

2605 

Blue shale 

5 

2740 

i—/ iiu vj ii**i vi — — — — — — — — 

White lime 

10 

2615 

Black shale 

5 

2745 

T T 111 IV/ 11I11V/ — — — — — — — — 

Hard lime 

5 

2620 

Blue shale 

5 

2750 

11 U 1 VI 11 111 V/ — — — — —— — — — 

White slate 

5 

2625 

Black shale 

15 

2765 

White slate 

20 

2645 

Top of lime, hard 

5 

2770 


Correlation:—This well located two miles west of the Transcontinental, 


penetrated limestone at 2,500 feet which, although no fossils have been 
secured from it, is almost certainly to be correlated with the lime in the 
Transcontinental well. The lime in the Doan well made only a negligible show- 
of oil and was not shot. 


Magnolia Petroleum Co. No. 1, SB. cor. sec. 12, T. 4 N., R. 5 B 
Pontotoc County, Oklahoma. 

Ground elevation, 937 feet. 


1 

CHARACTER OF ROCK. | 

1 

Thick- | 
ness | 

1 Feet 1 

Depth 

Feet 

1 

CHARACTER OF ROCK. | 
1 

Thick- | 
ness | 
Feet | 

Depth 

Feet 

Sand 

15 

15 

Hard sand 

10 

1205 

UA11U-—-— — — — — 

OnirL qqhH 

15 

30 

White slate 

70 

1275 

W U i C iV o U 1 I U — — — — 

Limey sand 

30 

60 

Lime shell 

10 

1285 

R pH hpH 

130 

1 60 

Slate 

3 

1288 

1\CU ucu-—- 

W qfpK cqnd 

90 

250 

Sand 

12 

1300 

YY did od.HU. — —- 

Chpll and shale 

110 

360 

Slate and shell 

170 

1470 

oiicii diiu oiidit/- 

Watpt* sand 

30 

390 

Black gumbo 

135 

1605 

YVdlCl O d 11 LI- 

Slate and shell- 

70 

460 

Sand 

10 

1615 

Wq fp k cond 

20 

480 

Brown shell 

145 

1760 

YY did odliU- 

Q1 ct t p 

160 

640 

Sand 

130 

1870 

OldlC-—- 

Water sand 

10 

650 

Slate and shell- 

210 

2080 

Slate 

80 

730 

Brown shale 

20 

2100 

X\J ofpK cond 

30 

760 

White lime 

50 

2150 

YY dlCI odHU-— -— 

R1 o r*lr cViciIp 

100 

860 

Sand 

5 

2155 

DIdLK. on a 1 c- 

Uayd 11 m p 

130 

990 

Blue slate 

45 

2200 

11 d i u nine-- 

"Whitp slate 

75 

1065 

Brown shale 

265 

2465 

YY 111 l C OldlC — — — — — — — — 
Wo v/1 Q Vl P 1 1 

5 

1070 

Hard lime 

35 

2500 

n d r u o 11 c 11 - 

Slate 

12 

1082 

Sand 

55 

2555 

Sand 

23 

1105 

Water sand 

| 205 

2760 

Oil show 



Sand and lime 

] 505 

3265 

nHv li tvl P 

40 

1145 

Blue slate 

1 45 

3310 

o d ii u j mile-- 

Slate and shell- 

50 

1195 


1 



Correlation:—In this well the formation from 1,870 feet to 2.1 So feet 


is doubtfully correlated as Hunton. 























































































166 


WELL LOGS 


Dayokla Oil and Gas Co. No. 1, Center sec. 16, T. 3 N., R. 6 B. 
Pontotoc County, Oklahoma. 

Ground elevation, 1073 feet. 


CHARACTER OF ROCK. 

Thick¬ 

ness 

Feet 

| Depth 
[ Feet 

1 

CHARACTER OF ROCK. 

Thick- | 
ness 
Feet 

Depth 

Feet 

Soil and mud 


5 

Soft sandy lime- 

6 

560 

Soft cellar 

5 

10 

More gas 



Red sandstone, soft _ 

10 

20 

Soft white lime- 

20 

580 

Hard blue slate_ 

8 

28 

Soft white slate_ 

5 

585 

Hard gray slate_ 

7 

35 

Soft white shale- 

20 

605 

Hard blue slate- 

5 

40 

Sandy gray shale_ 

55 

660 

Hard blue lime 

2 

42 

Sandy gray shale_ 

20 

680 

Medium gray slate_ 

8 

50 

Sandy gray shale_ 

55 

735 

Hard blue lime 

10 

60 

Hard white lime_ 

10 

745 

Soft blue shale 

4 

64 

Hard lime 

10 

755 

Hard blue lime- 

7 

71 

Hard sandy lime_ 

12 

767 

Hard sandy lime_ 

9 

80 

Hard sandy lime_ 

7 

774 

Medium black slate _ 

10 

90 

Little gas, sandy lime 



Hard sandy lime- 

8 

98 

looks good show of 



Hard sandy slate?_ 

2 

100 

gas 



Hard blue lime 

5 

105 

Hard sandy lime_ 

26 

800 

Hard blue lime 

2 

107 

Hard sandy lime_ 

10 

810 

Hard brown sand- 

8 

115 

Hard white lime_ 

15 

825 

Showing of gas 



Hard white lime_ 

15 

840 

Hard blue lime_ 

8 

123 

Hard white lime_ 

10 

850 

Hard black slate_ 

7 

130 

Hard white lime_ 

10 

860 

Hard gray slate_ 

15 

145 

Hard white lime_ 

5 

865 

Hard white lime_ 

4 

149 

Hard white lime_ 

10 

875 

Soft sandy shale- 

16 

165 

Hard white lime- 

10 

885 

Soft sandy shale- 

5 

170 

Hard white lime_ 

10 

895 

Hard white lime_ 

2 

172 

Hard white lime- 

15 

910 

Soft black shale_ 

28 

200 

Hard white lime_ 

10 

920 

Hard white lime_ 

2 

202 

Soft blue sand 

15 

935 

Soft sandy shale- 

98 

310 

Hole full water 



Medium brown shale 

25 

335 

Soft gray sand 

15 

950 

Bad cave 



Little oil in bottom 



Hard brown shale __ 

25 

360 

sand 



Soft gray shale 

40 

400 

Hard gray sand- 

5 

955 

Show of gas 



Hard brown sand- 

15 

970 

Soft gray shale 

20 

420 

Gray sand 

5 

975 

Soft brown shale- 

10 

430 

Gray sand 

10 

985 

Soft brown shale_ 

5 

43 5 

Hard gray sand_ 

15 

1000 

Soft brown shale- 

10 

445 

Sandy gray lime_ 

5 

1005 

Soft brown shale- 

5 

450 

Hard brown lime_ 

5 

1010 

Soft brown shale- 

35 

485 

Hard gray lime 

5 

1015 

Soft gray shale 

1 5 

500 

Hard gray lime 

4 

1019 

Hard gray shale- 

5 

505 

Hard brown lime_ 

3 

1022 

Hard gray shale- 

20 

525 

Hard white lime_ 

4 

1026 

Hard white lime- 

5 

530 

Hard sandy lime_ 

5 

1031 

Show of gas 



Hard white lime- 

5 

1036 

Hard white lime_ 

10 

540 

Hard gray shale_ 

4 

1040 

Just top of gas sand 



Show of oil 



making 4000 feet 



Hard Simpson sand _ 

28 

1168 

Soft gas sand 

10 

550 

Sand and shale inter- 



Soft white lime- 

4 

554 

stratified 

97 

1265 

Show of gas 



Black shale 

9 

12 74 






























Dayokla OH and Gas Co. No. 1, Center sec. 16, T. 3 N., R. 6 R. 
Pontotoc County, Oklahoma. 

Dayokla Oil and Gas Co. No. 1.—(Continued). 


CHARACTER OF ROCK. 

Thick¬ 

ness 

Feet 

Depth 

Feet 

1 

CHARACTER OF ROCK. | 

Thick¬ 

ness 

Feet 

Depth 

Feet 

Set 65/s" 



White sand and shale 

1 10 

1500 

Sandy lime 

9 

1283 

Lime and sand 

100 

1600 

Sand-water, sulphur 



Middle member of the 



water 

10 

1293 

Simpson sand 



Sandy lime 

3 

1296 

Dry, neither water or 



Asphalt sand 

29 

1325 

oil 

110 

1710 

White lime 

64 

1390 





Correlation:—In this well the rocks encountered from about 100 feet 


to 485 feet have been correlated as Caney and Woodford; those from 485 
feet to 580 feet as Hunton; those from 580 feet to 735 feet as Sylvan shale; 
those from 735 feet to 1,040 feet as Viola; and those from 1,040 feet to 
1,710 feet as the upper and middle members of the Simpson formation. 


Well No. 2, W. y 2 , of NR. %, sec. 18, T. 7 N., R. 5 R. 
Pottawatomie County, Oklahoma. 

Maud Oil & Gas Co. 


CHARACTER OF ROCK. 

Tnick- 

ness 

Feet 

Depth 

Feet 

1 

CHARACTER OF ROCK. | 

! 

Thick- | 
ness I 
Feet 1 

Depth 

Feet 

RpH rock 

30 

30 

Streaked shale I 

171 

560 

Watpr sand 

30 

60 

Lime shell 1 

141 

574 

TY U l L 1 JullU — — -- 

RpH rr>r*V 

10 

70 

Blue shale I 

61 

580 

i\CU 1 Utlv — — — — — 

Sandy shale 

25 

95 

Hard white sand-1 

141 

594 

H a r d •sand 

10 

105 

Red shale 1 

7 

601 

llul U OAUvt — — — 

Red mud 

5 

110 

Sandy blue shale_| 

311 

632 

Sandy blue shale- 

5o 

160 

Water, broken sand-- 

8| 

640 

Salt water sand- 

5 

165 

Sandy lime I 

2 01 

660 

R r rv \\t n Q Vi 1P 

25 

190 

Red shale 1 

71 

667 

DI UW 11 OllAlC - 

T? a H m i i H 

10 

200 

Blue shale _ 1 

231 

690 

I\CU ill uu- 

Sandy blue shale- 

40 

240 

Water sand 1 

2| 

692 

Blue and brown shale 

10 

250 

Blue shale 1 

8! 

700 

Sandy brown shale — 

6 

256 

Gray lime 1 

35| 

735 

Sand with water- 

14 

270 

Oil show—white sandl 

51 

740 

G Y'WTC* 1 

20 

290 

Blue sandy 1 

12 j 

752 

V_JI aVCl -- 

Dad m nd 

2 

292 

Brown sandy 1 

131 

756 

rVcU. Ill UU.-—- 

Qond 

38 

330 

Sand, light 1 

tol 

775 

Streaked brown and 



Blue shale 1 

211 

796 

blue - 

10 

340 

Dark coarse sand __| 

5| 

801 

Rlii* ckolp 

10 

350 

Blue shale 1 

51 

806 

DlUC Mlaic - 

Brown and red shale 

10 

360 

Sandy lime I 

141 

820 

Red muddy shale- 

10 

370 

Light shale I 

5| 

825 

Red shale 

10 

380 

Sand hard, parafine 1 

1 


D 1,, A c lio 1 P 

1 7 

397 

and oil 1 

3 81 

863 

DlUc SiMIc- 

Hard white sand- 

2 

399 

Red shale 1 

7| 

870 

Blue and brown- 

4 

403 

Mixed shale 1 

151 

885 

Pad cli'ilp 

17 

420 

Lime shell 1 

6 51 

950 

I\cli Mlaic - 

Blue and brown shale 

10 

430 

Red rock 1 

31 

953 


20 

450 

Sandy lime 1 

81 

961 

rUi6 reel mu a - 

Brown and red shale 

10 

460 

Blue shale 1 

71 

968 

Blue and brown shale 

30 

490 

Sandy lime shell - 1 

38| 

1006 

Soft blue shale 

20 

510 

Blue and brown shale 1 

2l 

1008 

Gray sandy slate - 

1 5 

525 

Water and sand-1 

2 71 

103 5 

Sand, little water - 

10 

535 | 

Sandy lime 1 

51 

1040 

Red shale - 1 

8| 

543 i&l 

Red rock 1 

5o| 

1090 












































































Well No. 2, W. y 2 , of NB. %, sec. 18, T. 7 N., R. 5 B. 
Pottawatomie County, Oklahoma. 

Maud Oil & Gas Co.—(Continued). 


[ 

CHARACTER OF ROCK. | 
1 

Thick- | 

ness 

Feet 

Depth 

Feet 

1 

CHARACTER OF ROCK. | 
1 

Feet | 

ness | 
Thick- | 

Feet 

Depth 

Blue shale 

5 

1095 

Red rock 

5 

2150 

Blue shale 

20 

1115 

White lime 

10 

2160 

Sand hole full water.. 

10 

1125 

Blue gravel 

10 

21 70 

Sand blue shale- 

7 

1132 

Light gray shale- 

20 

2190 

Sand 

IS 

1147 

Black slate 

130 

2320 

Rlup shalp 

18 

1165 

Hard sand 

5 

2325 

Lime shell 

16 

1181 

(Small lime shale 



Brown shale 

4 

1185 

on top of slate— 



Brown shelly shale __ 

10 

1195 

no water) 



Blue shelly shale- 

45 

1240 

Slate 

75 

2400 

Blue shelly shale _. 

15 

1255 

Lime shell 

5 

2405 

Blue shelly shale_ 

55 

1310 

Sand 

10 

2415 

Sandy limp 

80 

1390 

Slate . 

30 

2445 

Blue shale 

15 

1405 

Lime 

5 

2450 

Red shale 

25 

1430 

Sand, dry, no water 

10 

2460 

Rlup shalp .. 

20 

1450 

Black sand 

25 

2485 

Shelly blue shale- 

5 

1455 

Gray shale 

15 

2500 

Blue shale 

20 

1475 

Rlup shalp 

60 

2560 

Sand—little water __ 

45 

1520 

Sand salt water- 

25 

2585 

Sandy shalp - - 

1 6 

1536 

Broken slate 

29 

2614 

Blue shale 

34 

1570 

Gray shale 

31 

2645 

Blue lime 

40 

1610 

Slate _ _ _ 

30 

2675 

Rlup limp 

10 

1620 

Sand 

10 

2685 

Black sand 

5 

1625 

Sand 

5 

2690 

Brown mud 

20 

1645 

Lime 

18 

2708 

Hard sand 

25 

1670 

Lime and shale_ 

12 

2720 

Blue shale 

30 

1700 

Hard lime shell_ 

5 

2725 

Sandy lime 

5 

1705 

Sticky shale 

11 

2736 

Rlue shalp 

85 

1790 

Sticky shale 

5 

2741 

Pink shale 

10 

1800 

Sticky shale 

1 2 

2753 

Salt water—sa~d— _ 



Dark shale and shells 

17 

2770 

some gas 

10 

1810 

Hard shell 

6 

2776 

Hard sandy lime_ 

10 

| 1820 

Blue shale 

4 

2780 

Sand 

10 

1830 

Dark shale 

1 0 

2790 

Slate 

8 

1838 

Lime shell shale_ 

6 

2796 

Blue slate 

4 

1842 

Dark shale 

54 

| 2850 

Lime shell 

6 

1848 

Blue shale 

25 

2875 

Blue slate 

7 

1855 

Sticky shale 

35 

2910 

Black slate 

5 

1860 

Lime 

10 

2920 

White slate 

11 

1871 

Blue shale 

25 

2945 

Blue slate 

11 

1882 

Lime 

16 

2961 

Blue shale 

8 

1890 

Gas showing, sandy _ 



Gray lime 

5 

1895 

lime 

4 

2965 

Blue shale 

30 

1925 

Blue shale 

30 

2995 

Slate caves 

20 

1945 

Hard lime shell_ 

5 

3000 

Brown shale 

25 

1970 

Blue shale 

70 

3070 

Hard lime 

15 

1985 

Hard shale 

5 

3075 

Water sand—some_ 



Rlup shalp 

45 

3120 

water 

1 15 

2000 

Oil and gas showing, 



Blue shale 

1 65 

2065 

sand 

4 

3124 

Slate 

75 

2140 

Blue shale 

43 

3167 

Gravel 

| 5 

2145 

Sand, (show oil and 


































































































WELL, LOGS 


169 


Well No. 2, W. y 2 , of NB. %, sec. 18, T. 7 N., R. 5 B. 
Pottawatomie County, Oklahoma. 

Maud Oil & Gas Co.—(Continued). 


CHARACTER OF ROCK. 

Thick- 
| ness 

I Feet 

| Depth 
! Feet 

1 

CHARACTER OF ROCK. 

Thick- 
| ness 

1 Feet 

Depth 

Feet 

gas) water in bottoml 

85 

3252 

Blue slate 

8 

3468 

Blue shale 

90 

3342 

Show gas, lime shell 

6 

3474 

Show gas, lime shell 

6 

3348 

Brown slate 

26 

3500 

Blue shale 

17 

3365 

Dark blue slate- 

20 

3520 

Gas show—shell_ 

4 

3369 

Brown slate 

80 

3600 

Blue shale 

47 

3416 

Blue shale 

l 5 

3615 

Lime shale 

3 

3419 

Brown slate 

11 5 

3730 

Blue slate 

31 

3450 

Oil sand 

45 

3775 

Some water (3 bailers 



Blue green shale- 

19 

3794 

per hour) 



Hard shelly formation 

12 

3806 

Sandy shale 

10 

3460 

Blue shale 

16 

3822 


Correlation:—Shortly after the discovery of the limestone in the Trans¬ 
continental well considerable excitement was caused by the bringing in of 
the Maud Oil and Gas Company’s well, No. 2, located in sec. 18, T. 7 N., R. 
5 E., about 12 miles north of the Transcontinental well. The producing 
horizon at Maud was also found to be a limestone and resembled the bed in 
the Transcontinental well, in that it was only about So feet thick, but dif¬ 
fered from both the Nance and Transcontinental occurrences in that it was 
rather sandy. 

It is not known what significance attaches to the fact that the fossils 
from the Maud well indicate that the lime there belongs to the upper Hunton 
(Heldebergian) while those from the Nance well indicate that the formation 
at that place belongs to the lower Hunton (Niagaran). It may be that the 
apparent absence of portions of the formation in each locality is to be ex¬ 
plained as a mere coincidence in the writer’s selection of the few fragments 
which were sent to Dr. Galloway and Dr. Schuchert; or it may be that 
certain portions of the bed were more easily shattered and thus contributed 
a majority of the fragments available after the wells had been shot. 


Iowa Oil Refining Co. Center sec. 12, T. 3 N., R. 7 B. 
Pontotoc County, Oklahoma. 


Ground elevation, 841 feet. 


CII/.RACTER OF ROCK. 

| Thick- 1 
| ness | 

| Feet | 

Depth 

Feet 

1 

CHARACTER OF ROCK. | 

1 

Thick- 1 

ness | 
Feet | 

Depth 

Feot 

Soil, yellow shale- 

Clay 

1 

1 30 

20 

50 

Black shale 1 

White shale | 

lOl 

7o| 

225 

295 

Blue shale 

lOl 

60 

Lime shell i 

15! 

310 

Oil sand 

1 5| 

65 

Redbed _ | 

151 

325 

Rlii a Q’hfllp 

201 

85 

Blue shale 1 

51 

330 

Uiuc Oil ttl L-— — — 

Blue shale 

I 20l 

105 

Lime shell, sandy lime! 

1 o I 

340 

Dry sand 1 

1 55! 

160 

Soft red sand ! 

ioi 

350 

Blue shale 1 

1 55| 

215 

Hard oil sand | 

25 i 

375 













































Iowa Oil Refining Co. Center sec. 12, T. 3 N., R. 7 B. 
Pontotoc County, Oklahoma. 

Ground elevation, 841 feet.— (Continued.)• 


CHARACTER OF ROCK ' 

Thick¬ 

ness 

Feet 

Depth 

Feet 

CHARACTER OF ROCK j 

Thick¬ 

ness 

Feet 

Depth 

Feet 

White shale 

15 

390*1 

Sandy lime 

50 

2385 

RpH sand 

10 

400 

Sandy lime 

125 

2510 

Whitp shfllp 

5 

405 


Sandy lime 

35 

2545 


10 

415 


White lime 

10 

2555 

White shale 

25 

440 


Blue shale 

135 

2690 

Shale 

35 

475 


? 

16 

2706 

Hard lime 

15 

490 


White hard lime- 

84 

2790 

Sand 

10 

500 i 


Sandy lime 

20 

2810 

S h a1 p 

10 

510 


Brown lime 

65 

2875 

H arr\ «anH 

5 

515 


White lime 

65 

2940 

Whit' 3 sbalp 

10 

525 


? 

20 

2960 

Rpdbpd 

5 

530 


Water sand 

26 

2986 

^anr? chnw nil 

5 

535 


Sand 

29 

3015 

Shale 

15 

550 


Hard sand 

20 

3035 

Black limp 

1 0 

560 


Dry hard sand 

20 

3055 

Whitp shalp 

90 

650 


? 

1 

3056 

Hard sand 

25 

675 


Slate 

4 

3060 

Redbed 

20 

695 


Sand 

5 

3065 

Hard sand 

25 

7 9.0 


Hard sand 

15 

3080 

White shale 

40 

760 ! 

Hard lime 

10 

3090 

Blue shale 

1 80 

940 • 

White lime 

10 

3100 

Hard lime 

15 

955 

White, very hard lime 

10 

3110 

Blue shale 

20 

975 

White lime 

10 

3120 

Sand 

1 5 

990 

Lime 

10 

3130 

Water sand 

5 

995 

Sand 

15 

3145 

Hard sand 

13 

1008 

Lime 

3 

3148 

Lime 

1 7 

1025 

Lime 

4 

3152 

Blue shale 

40 

1065 

Water sand 

13 

3165 

Hard lime 

15 

1080 

Sandy lime 

15 

3180 

Blue shale 

85 

1165 

Sand 

12 

3192 

Hard lime 

25 

1190 

Sandy lime 

6 

3198 

Sandy lime 

30 

1220 

Hard sandy lime- 

5 

3203 

Blue shale 

25 

1245 

Sand 

8 

3211 

Sandy lime 

5 

1250 

Hard sandy lime_ 

11 

3222 

Water sand 

63 

1313 

Blue shale 

5 

322 7 

Dry sand 

87 

1400 

Sand 

7 

3234 

Sandy limp 

10 

1410 

Brown lime 

10 

3244 

Dry sand 

40 

14 5 0 

Blue lime 

20 

3264 

Blue shale _ 

450 

1900 

Blue lime 

21 

3285 

Rlark shalp 

40 

1940 

Blue very limp 

14 

3299 

Ypllnw shalp 

105 

2045 

Blue lime 

26 

3325 

Sandy lime _ 

45 

2090 

Top water sand- 

6 

3331 

Slate 

10 

2100 

Hard sand 

10 

3341 

Rm^n shalp 

100 

2200 

Sand 

5 

3346 

Red lime _ 

5o 

2250 

Soft sand 

10 

3356 

Sandy limp 

5° 

2300 

Sand 

52 

3408 

Water sand 

10 

2310 

Sand - 

8 

3416 

Hard lime 

15 

2325 

Sand 

10 

3426 

Shale - 

10 

2335 





Correlation:—In this well the formations from 1,410 feet to 1,940 feet 
are correlated as Caney and Woodford; those from 1,940 feet to 2,555 feet 
as Hunton; and the Sylvan from 2,555 feet to 2,706. 












































































































WELL LOGS 


171 


Hiram Jones No. 1, NW. Cor. sec. 16, T. 4 N. f R. 4 E., 
Pontotoc County, Oklahoma. 

Ground elevation, 1056 feet. 


CHARACTER OF ROCK. ' 

Thick¬ 

ness 

Feet 

Depth 

Feet 

1 

CHARACTER OF ROCK. | 
\ 

Thick- | 
ness | 
Feet | 

Depth 

Feet 

Hard sandstone_ 

25 

25 

Red bed 

8 

950 

Blue shale 

5 

30 

Blue shale 

5 

955 

Red bed 

30 

60 

Hard sand . 

5 

960 

Pink shale _ 

35 

95 

Hard sand 

15 

975 

Gray shale 

10 

105 

Gray shale 

10 

985 

Red bed 

10 

11 5 

Hard shell 

5 

990 

Blue shale 

10 

125 

Red bed 

38 

1028 

Red shale 

30 

155 

Hard white lime_ 

27 

1055 

Gray shale 

10 

165 

Red bed 

' 5 

1060 

Water sand 

10 

175 

Red bed 

5 

1065 

Red shale 

20 

195 

Hard sand 

20 

1085 

Blue shale 

85 

280 

Pink shale 

5 

1090 

Water sand 

10 

290 

Sand, water enough to 



Blue shale 

60 

350 

drill at 1095 

20 

1110 

Red shale 

15 

365 

Water sand 

5 

1115 

Gray shale 

10 

375 

Water sand, hole full 

15 

1130 

Red bed 

45 

420 

Red bed 

5 

1135 

Gumbo, sticky 

25 

470 

Water sand, hole full 

30 

1165 

Red bed 

20 

490 

Blue shale 

3 

1168 

Blue shale 

15 

505 

Hard sand 

2 

1170 

Blue shale 

5 

510 

Blue shale 

5 

1175 

Red bed 

10 

520 

Blue shale 

15 

1190 

1\ vu o ^ *-•** — —• — — — —• 

Hard lime 

14 

524 

Water sand, hole full 

20 

1210 

Red bed 

11 

535 

Dark blue shale_ 

30 

1240 

Pink shale 

35 

570 

Bed rock 

10 

1250 

1 1 1 1 IV J 1UUL-— — —-- 

Hard sand 

5 

575 

Shell _ 

3 

1253 

1 Idl U 0 cl 11 Li — — — —- 

Red bed 

45 

620 

Red rock 

7 

1260 

i\ vU O V- U —-— — — —- 

Hard lime 

15 

63 5 

Red bed 

15 

1275 

Red bed 

20 

655 

Red bed 

3 

1278 

i\CLl UCU-—- 

Rln a q h 9 1 p 

5 

660 

Lime _ _ _ _ _ 

12 

1290 

Uluc oliaiC — —- 

Red bed 

3 5 

695 

Blue shale _ _ 

15 

1305 

Red bed 

5 

700 

Water sand 

15 

1320 

l\CLi ULU —-— —- 

Red bed 

10 

710 

Hard fine sand 

10 

1330 

l\CH ULU---- 

Hard sandy lime - 

15 

725 

Water, hole full _ 

10 

1340 

R p /I 

20 

745 

Sand 

20 

1360 

1 \C u. ucu — —- 

Hard sandy lime - 

4 

749 

Blue shale 

10 

1370 

Red bed 

11 

760 

Black blue shale_ 

20 

1390 

Hard sandy lime - 

3 

763 

Blue shale 

15 

1405 

Ri’nnm chale 

7 

770 

Hard sand 

5 

1410 

DIUW11 ollaic-- 

25 

795 

Blue shale 

5 

1415 

I\ C Li UCU. -- 

Red bed 

10 

805 

Blue shale 

5 

1420 

Sandy lime 

5 

810 

Sand shell 

2 

1422 


5 

815 

Blue shale _ _ 

43 

1465 

i\ cli Ucll — —-—- 

F-T o conn 

8 

823 

Blue shale 

10 

1475 

nara sanu - 

Red bed 

67 

890 

Sandy lime and water 

15 

1490 

Rrourn C n O Ip 

20 

910 

Blue shale 

5 

1495 

Drown mi aic- 

/av con/i 

15 

925 

Blue shale 

47 

1542 

w aici Sana - 

5 

930 

Hard lime 

8 

1550 

orown snaie - 

P A 4 A 4 

5 

935 

Blue shale 

5 

1555 

i\cQ DcU- 

\i/1> {f a c li o Ip 

5 

940 

Hard lime 

5 

1560 

w nite snaie - 

Sand, show of asphalt 

2 

942 

Water sand 

5 

1565 












































































































172 


WELL LOGS 


Hiram Jones No. 1, NW., Cor. sec. 16, T. 4 N,, R. 4 B., 
Pontotoc County, Oklahoma. 


Hiram Jones No. 1,—(Continued). 


CHARACTER OF ROCK. 

Thick¬ 

ness 

Feet 

Depth 

Feet 

I 

CHARACTER OF ROCK. | 

Thicfc- 

| ness 
| Feet 

Depth 

Feet 

B|up shalp 

20 

1585 

White lime 

32 

1815 

Blue shale 

10 

1595 

I .i m e 

20 

1835 

Hard lime 

5 

1600 

Lime 

25 

1860 

Hard white lime_ 

25 

1625 

Lime 

60 

1920 

Yellow lime and. sand 



Lime 

35 

1955 

broken 

15 

1640 

Hard lime 

30 

1985 

Lim° 

20 

1660 

Green shale 

5 

1990 

Blue shale 

10 

1670 

Broken sand and 



Hard lime 

15 

1685 

black shale 

10 

2000 

Blue shale 

5 

1690 

Sand, water at 2015 

25 

2025 

Hard sand 

5 

1695 

Water sand 

15 

2040 

Water sand, sulphur 

5 

1700 

White shale 

10 

2050 

Hard sand, hole full 



White sand 

15 

2065 

of water 

10 

1710 

Sand 

30 

2095 

Hard sand 

5 

1715 

Water sand 

5 

2100 

Hard sand 

10 

1725 

Water sand 

15 

2115 

Water sand 

5 

1730 

Lime and green shale 

10 

2125 

Lime, hole full strong 



Sulphur water sand__ 

58 

2183 

sulphur water- 

30 

1760 

White sand and sandy 



Hard sandy lime- 

20 

1780 

lime 

67 

2250 

Pink shale 

3 

1783 

Quick sand 

17 

2267 


Correlation:—In this well the materials encountered from 1,360 feet to 
1,595 feet are correlated as Caney and Woodford; those from 1,595 feet to 
1,660 feet as part of the Hunton; and from about 1,990 feet to 2.250 feet as 
part of the Simpson. 


Vanoss Well, S. W. cor. sec. 34, T. 4 N., i?. 4 H. 
Pontotoc County, Oklahoma. 

Ground elevation, 982 feet. 


CHARACTER OF ROCK. 

| Thick¬ 

ness 

Feet 

Depth 

Feet 

CHARACTER OF ROCK. | 

1 

Thick¬ 

ness 

I Feet 

Depth 

Feet 

Sand and gravel_ 

44 

44 

White lime 

10 

190 

Whitp shalp 

14 

58 

Shalp 

55 

245 

White sand 

20 

78 

Red rock 

10 

255 

Red rock 

5 

83 

White shale 

45 

300 

Whitp limp 

5 

88 

Red rock 

5 

305 

White sand 

12 

100 

White shale 

5 

310 

Water pulled 110 



White lime _ _ 

28 

338 

barrels 



Water 



Shale - _ 

10 

120 

Red rock 

42 

380 

Sandy lime 

10 

130 

White lime 

5 

385 

Blue shale 

50 

180 

Red rock 

30 

415 






































































WELL LOGS 


173 


Vanoss Well, S. W. cor. sec. 34, T. 4 N., R. 4 B. 
Pontotoc County, Oklahoma. 

Ground elevation, 982 feet.— (Continued.) 


CHARACTER OF ROCK 

Thick¬ 

ness 

Feet 

Depth 

Feet 

CHARACTER OF ROCK 

Thick- 1 
ness 1 
Feet | 

Depth 

Feet 

White lime 

4 

419 

Blue shale 

•40 

834 

Red rock shale 

5 

424 

White lime 

20 

854 

White lime (hard)_ 

2 

426 

Blue shale 

20 

874 

White sand 

24 

450 

White lime 

10 

884 

Little showing 



White sand 

8 

892 

Light shale 

10 

460 

White shale 

2 

894 

Red rock 

64 

524 

White lime _ 

5 

899 

White sand 

12 

536 

Blue shale _ 

10 

909 

White shale 

10 

546 

Dark sand 

5 

914 

White sand 

100 

646 

.Sandy shale 

5 

919 

White shale 

10 

656 

White lime 

15 

934 

White lime 

5 

661 

Dark shale 

38 

972 

White shale 

2 

663 

Cap rock 

3 

975 

Lime 

15 

678 

Gray sand 

75 

1050 

Red shale 

22 

700 

Lime and. sand 

40 

1090 

1\ v V* OH wu. — — — — — — — — — 

Cavy 



White slate 

5 

1095 

White lime 

15 

715 

Lime _ 

10 

1105 

Red rock 

20 

735 

White sand water — 

35 

1140 

White sand 

10 

745 

White lime 

160 

1300 

Blue shale 

20 

765 

Lime 

560 

1860 

White sand and lime 

10 

775 

Hard lime 

100 

1960 

Red rock 

10 

785 

Sand 

120 

2080 

1\ O U 1 otiv-—-— 

Bluish sand 

9 

794 


1 



Correlation:—The lime encountered in this well from 1,140 feet to 
1,960 is correlated as Viola limestone, and the 120 feet of sand at the bottom 
of the well as Simpson. 




















































174 


PALEONTOLOGY 


PALEONTOLOGY 

GENERAL STATEMENT 

Almost 300 species and varieties of fossils have been collected 
and identified, from the formations that occur in the Stonewall 
quadrangle and that are above the Hunton terrane. Only the new 
species have been described, but most of the others have been fig¬ 
ured so that to those particularly interested in the area an oppor¬ 
tunity is afforded to check the identifications made by the writer. 

FAUNAL CHARTS 

Faunal charts have been constructed for most of the forma¬ 
tions and in addition a large general chart is included. In addition 
to the faunas of the Woodford to Stratford formation, inclusive, of 
the Stonewall quadrangle, the Pennsylvaniani faunas of Kansas, 
Texas, and Missouri, as well as that of the Morrow formation of 
Arkansas and Oklahoma, and the Mississippian faunas of the Moore- 
field and Batesville formations of Arkansas are shown on the general 
chart. A list of the more extensively used references are given at 
the end of the report. In the general chart reference is made to these 
by number, and a page, plate, and figure is given for each fossil 
listed. Reference is also made to the pages, plates, and figures 
devoted to the fossils, as described in the present report. 

DESCRIPTION OF NEW SPECIES 

The single genus and several species thought to be new are 
described. 


ANTHOZOA 


Genus CHAETETES Fisher 

CHAETETES SCHUCHERTI* n. sp. 

Description .— Corallum massive, irregular lense shaped, a few 
inches to two or three feet in diameter, frequently forming reefs. 
Base wrinkled, with very thin epitheca. The upper surface is undulat¬ 
ing, corallites long, prismatic, mostly five-sided, subequal, the same 
size throughout their length, averaging 3mm. in diameter, one 
diameter slightly longer than the other, opening normal to the 
surface. Apertures subpolygonal, with occasional septa-like inflec¬ 
tions due to fission and periodic swellings as if the walls were made 
up of rows of large granules. Walls completely amalgamated 
throughout their length, minutely granular, the outside not sharply 
defined, and made up of columns of granules directed obliquely up- 

* Named in honor of Professor Charles Schuchert of Yale University. 



PALEONTOLOGY 


175 


ward. In the corners between the corallites is a dark line. Walls 
not thickened by additions of secondary steroplasm; about 7mm. 
thick. Mural pores and septa absent. Tabulae nearly flat, very 
thin, and few in numbers, averaging not over one in 10mm. Some¬ 
times there is a zone in which adjacent corallites have 5 or 6 tab¬ 
ulae, above and below which tabulae are absent. Some tabulae are 
incomplete, possibly due to imperfect preservation. 

Multiplication of corallites is by fission. Scattered through 
the corallum are short round tubes without walls, 3mm. in diame¬ 
ter, filled with calcite, parallel with the corallites, and around which 
the corallites are much smaller and thicker walled. The corallites 
radiate outward from the tubes to a distance of 5 to 10 mm. and 
then turn upward. The tubes may have been centers of reproduc¬ 
tion, goniophores, or they may have been parasitic animals. They 
are best shown upon weathered surfaces. 

Remarks :—This species differs from C. milleporaceous in the 
smaller number of tabulae, thicker walls, and the presence of the 
sporadic tubes. 

Horizon and Locality :—In the northeastern part of the Stone¬ 
wall quadrangle the Homer limestone member of the Holdenville 
formation constitutes a reef which is almost entirely made up of 
this species. The form has also been identified from conglomeratic 
strata exposed in the old asphalt pit which is located near the center 
of the south line of sec. 20, T. 2 N., R. 6 E. The beds here exposed 
have previously been described as Franks conglomerate, but on the 
evidence afforded by the presence of this fossil, and with the addi¬ 
tional evidence contributed by a number of other species present in 
the same collection the conglomeratic strata here exposed are con¬ 
fidently correlated with the Holdenville formation. 


Genus PACHYPORA Lindstrom 

PACHYPORA CANEYANA n.sp. 


Description. —Corallum large, several specimens found with 
a length three inches and a width of one inch; form sub-cylindrical 
and ramose. Corallites prismatic, polygonal, and with diameters 
ranging from two to three mm. Walls of corallites thickened to¬ 
ward their mouths by layers of steroplasm. Calyces with width 
greater than depth. Tabulae thin in axial portion, two or three in 
the space of a diameter; away from the axial portion often thick¬ 
ened and generally more closely spaced; usually straight, but some¬ 
times bent sharply downward at centers; in a few instances arching 


176 


PALEONTOLOGY 


diagonally from the corallite wall to some portion of the preceding 
tabula. Mural pores few. 

Remarks .—This form somewhat resembles P. carbonaria Math¬ 
er, but may be distinguished from that species by the number and 
shape of the tabulae. 

Horizon .—The species is founded on a number of specimens 
found, however, at only one locality near the top of the Caney 
shale. Station 170. 


BRYOZOA* 

Genus ACANTHOCLEMA Hall 

ACANTHOCLEMA CARBONARIUM n.sp. 

Plate XXXVI, figs. 1, and 2. 

Description .—The zoarium forms slender ramose solid stems 
\ l / 2 io 2 mm. in diameter. The zooecia are thick walled, and 
arranged in diagonally intersecting series with 7 to 7 y 2 in 2 mm. 
The walls are marked by spiniform tubuli irregularly arranged in 
1 to 3 rows. In some parts of the section they are few. Their 
cross section varies in size from granules to >4 the short diameter 
of an aperture. A large acanthopore-like spine occurs at the basal 
end of the greater apertural diameter. 

The zooecial tubes bend outward at a large angle from the 
medial filiform axis to the vestibular zone where an additional out¬ 
ward turn cause the zooecia to approach the surface at right angles. 
Diaphragms are very rare, usually absent. 

This is the only species of Acanthoclema described from the 
Pennsylvanian, to our knowledge, and no difficulty should be en¬ 
countered in separating this form from the earlier Palaeozoic species. 

Occurrence .—Upper Savanna, locality 15, Stonewall quad¬ 
rangle, Oklahoma. 

Holotype. —Numbers 110-23 Columbia University, New York 

City. 


Genus FISTULIPORA McCoy 

FISTULIPORA SUTILIS n.sp. 

Plate XXXVII, fig. 2; Plate XXXVIII, figs. 1, and 2. 

Description .—The zoarium forms flabellate expansions 1 to 1 >4 
mm. Maculae of numerous vesiculae appear on the surface separ- 

*Dr. H. N. Coryell is responsible for the identification and description 
of the Bryoza. 



PALEONTOLOGY 


177 


ated 3 to 4 mm. apart. The zooecia are rounded with broad, lun- 
arium 4 to 5 in 2 mm. The interspaces vary from ^ to 1 aperture 
diameter in width outside of the macular areas, filled with one or 
two rows of vesiculae. 

The zooecial tubes are short, at first prostrate, upon the med¬ 
ian membrane. They attain full size early and curve rapidly to¬ 
wards the surface, reaching the periphery with a broadly acute 
angle. The apertures are distinctly hooded. The interspaces in 
the longitudial section are crowded with thick walled vesiculae mak¬ 
ing a nearly solid tissue filling at the surface. 

The bilaminate zoarial growth and the thick walled numerous 
vesiculae distinguish this species from other described forms. 

Occurrence .—Upper Francis formation, locality 228, Stone¬ 
wall quadrangle, Oklahoma. 

Holotype. —Numbers 111-23, Columbia University, New York 

City. 


Genus GLYPTOPORA Ulrich 

GLYPTOPORA INCRUSTANS n. sp. 

Plate XXXVII, fig. 5. 

Description .—The zoarium is an incrusting thin laminate form; 
the surface is covered with cup-shaped cavities made by bifurcating, 
and coalescing sharp ridges composed of layers of zooecia grown 
back to back. The laminae vary from y 2 \o \y 2 in. in thickness 
The “cups” have a maximum depth of 3 mm. and a diameter vary¬ 
ing from 2 to 10 mm. 

Scattered over the surface are variable shaped depressed solid 
maculae, the greater width varying from 1 to 1 y 2 mm. The zoo¬ 
ecia have sub-circular apertures surrounded by an unequally elevated 
peristome. From 5 y 2 to 6 occur in 2 mm. The method of growth 
distinguishes G. incrustans from the flabellate group. 

G. michelinia and G. incrustans are the only two described spe¬ 
cies that have incrusting zoaria. The thin laminae and greater 
variability in the size of the “cups” separates the latter from the 
former. 

Occurrence. —Wapanucka limestone, locality 23, Stonewall 
quadrangle, Oklahoma. 

Holotype. —Columbia University, New York City. 

GLYPTOPORA STONEWALLENSIS n. sp. 

Plate XXXVII, fig. 6. 

Description. —The zoarium of this species belong to the G. 


178 


PALEONTOLOGY 


keyserlingi group of Ulrich. It is represented by a fragment of the 
broad bifoliate ridge The surface is marked by acutely elliptical 
maculae arranged in a digitate pattern. The maculae are sur¬ 

rounded by zooecia larger than the normal size. Their length and 
width average 3 >4 and mm. respectively. The zooecial aper¬ 
tures are raised above the surface by a tubular peristome. In the 
tangential section the lunarium is quite distinct. The zooecia are 
from 1 y 2 to 2 diameters apart; 5 in 2mm. the interspaces are crowd¬ 
ed with vesiculae which at the surface are filled with solid tissue. 

The smaller size of the dimple-like maculae and the greater 
number of zooecia in 2 mm. distinguishes this species from other 
described forms. 

Occurrence. —Upper Francis formation, locality 228, Stone¬ 
wall quadrangle, Oklahoma. 

Holotype. —Numbers 111-16, Columbia University, New York 

City. 


Genus RHOMBOPORA Meek 

RHOMBOPORA SUBCRASSA n. sp. 

Plate XXXVIII, figs. 8, 9, and 10. 

Description .— The zoarium is ramose, branching at intervals of 
8 to 15 mm. The stems vary from 3 to 6 mm. in diameter. Aper¬ 
tures are rounded, separated about their diameter apart, and have 
thick walls that are dotted with 1 to 3 rows of spiniform tubuli. A 
iarge acanthopore is present between the zooecia, sometimes quite 
concealed by the numerous dark spots. There are 6 to 8 zooecia 
in the longitudinal rows in 2 mm. Mesopore-like interspaces appear 
in parts of the section. 

In the longitudinal section the tubes in the axial region have 
thin walls and bend obliquely toward the surface immediately after 
development. The mature region averages 1 mm. thick. The 
spiniform tubuli originate in the early part of the zone and extend 
to the surface. Diaphragms are few or absent. 

This species is distinguished from R. crassa Ulrich by the pres¬ 
ence of large acanthopores. The thick walls and well developed 
mature region will separate it from other described species. 

Occurrence. —Lower Francis, locality 116 Stonewall quad¬ 
rangle, Oklahoma. 

Holotype. —Numbers 110-25 Columbia University, New York 

City. 


PALEONTOLOGY 


179 


Genus STENOPORA Lonsdale 

STENOPORA BOGGYENSIS n. sp. 

Plate XXXIX, figs. 2, 3, and 4. 

Description .— The zoarium consists of ramose, sub-cylindrical 
solid stems 4 to 8 mm. in diameter. Maculae and monticules are 
absent. The zooecia are thick walled, and the apertures rounded. 
There are 9 in 2 mm. Mesopores are very few. 

In the tangential section the zooecia appear with thick or thin 
walls and sometimes with both variations due to the changes in posi¬ 
tion of the periodic thickenings relative to the plane of the section. 
An excessive constriction of the aperture occurs when the perforated 
diaphragms lie in the plane of the section. The division lines be¬ 
tween the zooecia are marked by a single row of dot-like thicken¬ 
ings in both the thick and thin walled areas. In the latter area 
beaded structure results. Large acanthopores, with a minute central 
lumen occur at the junction angles of the zooecia. The acantho¬ 
pores are about as numerous as the zooecia. 

The walls of the zooecia in the axial region are slightly crenu- 
lated and thickened with elongated-pouched swellings averaging one 
tube diameter apart. Diaphragms occur at periodic intervals of 
about 1 ^2 mm. the thickenings increase in number and size, the 
diaphragms become more numerous (4 to 5 in 1 mm.) and a few 
large acanthopores appear. 

The submature area differs from the axial region only in an 
increase in number of swelling and diaphragms. The mature and 
submature zone is \ J / 2 to 2 mm. thick. 

In the mature zone there are 9 to 13 thickenings and 9 to 10 
diaphragms in 1 mm. In every case the diaphragms form a hori¬ 
zontal base over which the tissue was deposited to a depth of y 2 
tube diameter, decreasing the zooecial cavity to the size of the 
perforated opening. A longitudinal section cut to one side of the 
aperture shows the excessive reinforcing tissue occurring through¬ 
out the mature area. 

A peculiar structure of very minute (1/40 mm.) spines pro¬ 
jecting downward from the zooecial border of the thickening are 
more distinctly visible here than in any species yet studied. 

S. boggyensis is more similar to S. ohioensis Foerste than any 
ether Pennsylvanian form. The greater thickening in the mature 
region, the occurrence of diaphragms, and thickenings in the axial 
region will distinguish this species from Foerste’s. 

Other Coal Measure forms have much larger zooecia than S. 
boggyensis. 


180 


PALEONTOLOGY 


Occurrence. —Boggy formation, locality 169, Stonewall quad¬ 
rangle, Oklahoma. 

Holotype. —Numbers 110-13, Columbia University, New York 

City. 

STENOPORA BULLATA n. sp. 

Plate XXXIX, figs. 5, and 6. 

Description .— The zoarium. consist of superimposed laminae 
forming bulbose masses that reach a known maximum of 3cm. 
high and 4 cm. broad. Each laminae varies from 1 to 4 mm. thick 
with a concentrically wrinkled basal epitheca. Eight to nine 
maculae occur in 1 sq. cm. The zooecia are thin and thick walled, 
7 to 8 in 2 mm. Almost every zooecia will show both variation. 
The small acanthopore-like dots that are quite numerous in many 
species are few here, only evident in the thicker walls. The 
acanthopores are variable in size, distinct, with small lumen, and 
inflect the apertural walls; three to seven are present about each 
zooecia. The large acanthopores originate promiscuously through¬ 
out the lamina and extend for only % to y mm. There are 13 to 
18 beaded swellings in 1 mm. A number of the beads project dia- 
phram-like out into one of the adjacent zooecial cavities. Dia¬ 
phragms occur throughout the zooecial tubes, from ^ to 2 tube- 
diameters apart. The zooecia rise from the basal membrane and 
lie prostrate for y 2 to mm. At that point a short upward turn 
and an increase to mature size is made. 

The numerous small beaded swellings and strongly inflecting 
acanthopores distinguishes this species from any other described 
species. 

Occurrence.— Wapanucka limestone, locality 31. Stonewall 
quadrangle, Oklahoma. 

Holotype. —Numbers 110-4 Columbia University, New York 

City. 

STENOPORA CIRCINA n. sp. 

Plate XL, figs. 2, 3, and 4. 

Description .— The zoarium consists of an incrusting lamina, 1 
to 3 J / 2 mm. thick. 

The type surrounds a crinoid stem and forms a cylindrical hol¬ 
low stalk 10 to 25 mm. in diameter. The size and shape varies 
with the shape of the foreign body. Maculae and monticules are 
absent. The zooecia are rounded, thick walled, and 8 to 9 in 2 mm. 
Mesophores are rounded and angular, and about as numerous as the 
zooecia. A distinct row of small dark spots mark the center of the 
wall about the apertures of both the mesopores and zooecia except 
in the deeper part of the tangential section. Acanthopores are large, 


PALEONTOLOGY 


181 


distinct, with a minute lumen, and located at the angles of contact. 
One to three occur about a zooecial aperture. 

The tubes rise from a thin basal tissue and for a short distance 
(A to y 2 mm.) lie prostrate. One to three complete diaphragms 
occur in the early part of the zooecia. In the first 1 y^ mm. above 
the abrupt outward bend the thickening is large and robust, 4 to 5 
in 1 mm. In the remainder of the lamina there are from 7 to 8 
elongated beaded thickenings and one to two thin diaphragms. 

These species differ from 5. micropora in having less number 
of mesopores, more distinct row of dark spots, initial prostrate tube 
and the variable change in number and distribution of thickenings. 
S. circina will rarely be confused with other described carboniferous 
forms. 

Occurrence .— Wapanucka limestone, locality 31, Stonewall 
quadrangle, Oklahoma. 

Holotype. —Numbers 110-10 Columbia University, New York 

City. 

STENOPORA HISPIDA n. sp. 

Plate XLI, figs. l,and 2. 

Description .— The zoarium consist of superimposed laminae 
that vary in thickness from 1 to 1 ^2 mm. It is usually found in- 
crusting crinoid stems. The surface is undulating and spinose with 
an occasional knob-like branch rising 5 to 8 mm. high. Maculae 
of larger apertures, 4 to 5 mm. apart are present. 

The zooecia are rounded, thick walled and surrounded by 4 
to 8 large acanthopores. The median division is marked by a light 
line. There are 7 to 7 y 2 zooecia in 2 mm. Mesopores are absent. 
The tube rises almost directly from the basal membrane. The bead¬ 
ed thickenings are few, 3 or 4 occurring through a tube length. 
Complete and perforated diaphragms vary from y 2 io \y 2 tube 
diameter apart unaccompanied by the addition of secondary thick¬ 
ening. The great number of large acanthopores, the absence of 
mesopores and row of minute dark spots, and the zoarial growth 
serves to distinguish this species from other described Stenopora 
forms. 

Occurrence .— Wapanucka limestone, locality 31, Stonewall 
quadrangle, Oklahoma. 

Holotype. —Numbers 110-9 Columbia University, New York 

City. 

STENOPORA MACALESTERANA n. sp. 

Plate XL, figs. 6, and 7; Plate XLI, fig. 3. 

Description .— Zoarium is ramose, subcylindrical solid stems 8 


182 


PALEONTOLOGY 


to 16 mm. in diameter. Distinct maculae and monticules are ab¬ 
sent. The zooecia are thick walled with rounded apertures and 7 
to 8 in 2 mm. Mesopores are very few and only occasionally 3 or 
4 are found around a zooecium that is slightly above normal size. 

In the tangential section the zooecia have the wall variation 
described under S. boggyensis. The division line between the zoo- 
ecial walls is marked by a row of more distinct and larger thicken¬ 
ings than in that species. There are from one to three large acan¬ 
thopores about each zooecia, occurring at the junction angles. A 
lumen is usually visible in the center of each large spine. 

Diaphragms are rare in the axial region, one or two were ob¬ 
served at a horizon of rejuvenation. The periodic thickenings in 
the immature zone are “fuzzy,” elongate, 3 to 4 tube diameters 
apart, and occurring in zones throughout the immature region. 

In the submature area, a series of large short (J4 to Yz mm.) 
acanthopores arise. 

The thickness of the mature region equals ^ to ^ of the 
diameter of the zoarium. Thickenings occur throughout this zone; 
9 to 10 in 1 mm. The appearance of the swellings are similar to 
those of S. boggyensis. Four to seven diaphragms cross the zooecial 
tubes in 1 mm. The large zooecia, absence of diaphragms and 
conspicuous thicknings in the axial region, and the more robust 
zoarial growth, distinguishes this species from S. boggyensis. 

The more massive thickenings in the mature region and larger 
zooecia separate S. macalesterana from S. ohioensis Foerste. S. car- 
bonariz var. conferta has much larger zooecia and less dense beaded 
structure than S. macalesterana. 

Occurrence .— Upper McAlester formation, locality 16, Stone¬ 
wall quadrangle, Oklahoma. 

Holotype. —Numbers 110-7 Columbia University, New York 

City. 

STENOPORA MICROPORA n. sp. 

Plate XLI, figs. 4, and 5. 

Description .— The zoarium consists of laminar expansion 1 to 
2 mm. thick incrusting foreign objects. (The type surround a crin- 
oid stem.) The surface is spinose without maculae or monticules. 
The zooecia are rounded, either in contact with one another or sep¬ 
arated by a distance equal to their diameter. Nine adjacent zooecia 
occur in 2 mm. The interspaces are crowded with angular and 
rounded mesopores which are twice as numerous as the zooecia. 
Targe, distinct acanthopores traverse two-thirds of the laminar zoar¬ 
ium, and project from y 2 to 1 mm. above the aperture in well pre¬ 
served specimens. Dense tissue forms a dark spot around the 


PALEONTOLOGY 


183 


minute central lumen. Few unequal spaced, minute acanthopore- 
like structures appear along the division of the walls. They may be 
absent or as many as three along the contact area of two adjacent 
zooecial tubes. 

Nine to ten ring-like swellings occur in 1 mm. length of a zoo¬ 
ecial tube. The swellings extend outward and downward from the 
wall with a pouched or beaded appearance and do not indicate the 
presence of a perforated diaphragm. The zooecial tubes are usually 
crossed by 1 to 3 diaphragms. In a few of the zooecia diaphragms 
are absent. The great number of mesopores, the scattered distribu¬ 
tion of the interzooecial dark spots, and the pouched and merged 
swelling, distinguishes this species from any other described from 
the Pennsylvanian. 

Occurrence. —Wapanucka limestone, locality 31, Stonewall 
quadrangle, Oklahoma. 

Holotype .— Numbers 110-1 Columbia University, New York 

City. 


STENOPORA WAPANUCKAENSIS n. sp. 

Plate XLI, figs. 7, and 8. 

Description .—The zoarium consists or ramose, compressed cyl¬ 
indrical solid stems 6 to 12 mm. in diameter. Three distinct mac¬ 
ulae of large zooecia occur in Y sq. cm. The zooecia are poly¬ 
gonal, thick walled, 7 to 8 in 2 mm. Mesopores are few to wanting. 

In the tangential section the variable wall structure is less pro¬ 
nounced, the thin walled types scarcely show. A single row of dark 
spots mark the division of the zooecial wall except in the maculae 
where two rows are frequently present. Two to four large acantho- 
pores surround a great number of the zooecia. The diameter of the 
larger ones is equal to the aperture of a perforated diaphragm. 

The walls of the axial region are coarse and slightly crenulated. 
Diaphragms are absent. The mature region has a thickness of 2 
mm. in the type specimen. Beaded and diaphragm thickenings oc¬ 
cur closely crowded, and usually merged into one another; 6 to 7 
in 1 mm. Three to five diaphragms in 1 mm. cross the zooecial 
tube. In most cases they form the horizontal bases of the secon¬ 
dary tissues deposit. 

The larger and merging appearance of the beaded and dia¬ 
phragm-thickenings and the less robust size distinguishes S. wapa- 
nuckaensis from S. boggyensis, S. macalesterana and S. onhioensis. The 
more regular thick walled character separates S. wapanuckaensis 
from S. carbonaria and its varieties which occur in the Pennsylvan¬ 
ian strata. 


184 


PALEONTOLOGY 


Occurrence. —Wapanucka limestone, locality 160, Stonewall 
quadrangle, Oklahoma. 

Holotype. —Numbers 110-8 Columbia University, New York 

City. 


BRACHIOPODA 

Genus PRODUCTUS Sowerby 

PRODUCTUS GALLOWAYI n. sp. 

Description .— Above medium size, attaining a length of two 
inches. Shell longer than wide; ratio of width to length averaging 
2/3. Hinge margins slightly less than greatest breadth of shell; ears 
prominent, thin and therefore generally broken; marked by several 
wrinkles that become obsolete before passing far inward upon the 
side of the shell. Posterior portion of ventral velve rather uniform¬ 
ly convex, slightly incurving; anterior portion straightened. The 
beak projects well beyond the cardinal border and is slightly in¬ 
curved. 

Surface of shell marked by fine rounded striae that increase 
in number and decrease in size anteriorly. The number of umbonal 
striae decreases anteriorly by termination at the base of a few rather 
large, sub-medial spines. With the decrease anteriorly of the 
number of medial umbonal striations, however, many new lateral 
striae are evolved by implantation and the total number increases 
with the growth of the shell. The operation of this process results 
in a convergence of the striae along the central part of the valve and 
generally, apparenly because of crowding, in the formation of a 
ventral fold. The formation of a fold rather than a sinus on the 
ventral valve suggests a relation of this species with P. insinuatus 
Girty. The two are to be distinguished, however, by the much 
greater relative length of P. gallowayi and by the manner of decrease 
of medial striae in this species. 

Occurrence .— Known only from a number of ventral valves 
collected from the Wapanucka limestone. Named in honor of 
Professor J. J. Galloway of Columbia University. 

Holotype .—Columbia University, New York City. 

PELECYPODA 

Genus CONOCARDIUM, Bronn 

CONOCARDIUM SNIDERII n. sp. 

Description. —Shell large; length about twice as great as height; 


PALEONTOLOGY 


185 


anterior side truncated with forward slope and flattened so as to 
present a regular heart-shaped outline when viewed from in front; 
length of anterior auricle unknown. Base long, sinuous, sloping 
up so as to intersect the hinge line at an angle of about 40 degrees; 
widely gaping, posterior valve edges crenate. Beak not projecting 
beyond hinge line; umbonal slopes prominent, rounded and directed 
obliquely forward. Surface ornamented with strong, sharply-ele¬ 
vated, radiating ribs that are of the same number from the umbo 
to the posterior margin; three ribs on the umbonal slope slightly 
larger than the others. The radiation of the ribs and the lack of 
secondary ribs results in an increase in the width of the interspaces 
from less than a rib-width cn the umbo to as much as four times a 
rib-width at the posterior margin. Surface also marked by strong 
but discontinuous concentric striae which with the ribs produce a 
cancellated sculpture. 

In shape this species resembles Conocar di-urn obliquum Meek and 
Worthen. It is easily distinguished from that form, however, by its 
greater size, more sinuous base, and more pronounced marking. 

Horizon .— Upper part of the Caney shale. Named in honor 
of Dr. L. C. Snider, chief geologist for the Empire Gas and Fuel 
Company. 

Holotype. —Columbia University, New York City. 

CEPHALOPODA 

FamPy AGANIDIDAE 
Genus DRYOCHOCERAS n. gen. 


Description .— Form discoidal, involute, laterally compressed. 
Cross section of the whorl high and narrow with flattened sides and 
acute venter. The umbilicus is small. The height of the whorl is 
slightly more than one half the diameter of the shell, the ratio being 
15/27; greatest width of whorl one-third the diameter of the shell. 
Surface ornamentation known for only a small area on the genotype. 
This shows fine sigmoidal ribs which bend backward toward the 
venter. 

Sutures sub-parallel; lobes angular; saddles rounded; ventral 
lobe undivided. 

Genotype .— Columbia University, New York City. 

GENOTYPE 

DRYOCHOCERAS BRAINERDI n. sp. 

Description .— Discoidal, laterally compressed, strongly invo- 


1S6 


PALEONTOLOGY 


lute; whorls high and narrow with acute venter; ratio of height of 
whorl to diameter of shell is 15/27; ratio of greatest width of whorl 
to diameter of shell is The umbilicus is small with a sharp 
shoulder. Surface ornamentation as shown by a small area pre¬ 
served on the genotype consists of fine sigmoidal ribs that bend 
backward toward the venter. 

Sutures sub-parallel. The ventral lobe is sharp and undivided; 
superior-lateral saddles relatively narrow and rounded; superior- lat¬ 
eral lobes angular with an average angle of about 45 degrees; sec¬ 
ond lateral saddles slightly rounded, somewhat broader than preced¬ 
ing lobe; second lateral lobe angular also broader than either the 
ventral or superior-lateral lobes; third lateral saddle broadly round¬ 
ed terminating at the umbilical shoulder. 

Occurrence .— This genus and species is at present known only 
from the basal part of the Caney shale. (See chart of the Caney 
fauna). Named in honor of Mr. A. E. Brainerd who ably assisted 
the writer in the field investigation upon which the present report 
is based. 

Holotype .— Columbia University, New York City. 


PALEONTOLOGY 


187 


PLATE XXIX 



FUSILINA SECALICA (Say) 

Figs. I and la. Longitudinal and cross sections of a number of specimens 
from the Homer limestone member of the Holdenville formation. Sta¬ 
tion 127, x 3 l/l0. 



1S8 


PALEONTOLOGY 



PLATE XXX 

AULOPORA PROSSERI Beede 

F : g. 1. 

View from above. 

la. 

View of base. 

lb. 

Cross section x 3. Holdenville forma ion, station 23u. 

Fig. 2. 

CAMPOPHYLLUM TORQUIUM (Owen) 

Cross section x 2 1/2. 

2a. 

Longitudinal section x 2 l/2. 

2b. 

Side view of average sized specimen. Boggy formation station 
171. 


PLATE XXX 
















190 


PALEONTOLOGY 


PLATE XXXi 

CHAETETES MILLEPORACEUS Milne-Edw ards and Haime 

Fig. l. Tangential and cross sections, x 3 l/2 Holdenville formation, 
station 216. 

CHAETETES SCHUCHERTI n. sp. 

Fig. 2. Cross and tangential sections showing sporadic tube, x 3 l/2. 
2a. Top view of surface showing tube, x 3 1 / 2 . 

2b. View of surface. Natural size. Holdenville formation, station 
216 . 

CLADOCHONUS FRAGILIS Mather 

Fig- 3. 


Fragment of corallum x 3. Waranucka formation, station 28 . 


PLATE XXXI 




















192 


PALEONTOLOGY 


Fig. 1. 

PLATE XXXII 

CYTHAXONIA sp. 

Longitudinal section x 3 Vi 

la. 

Cross section near top of corallum x 3^ 


lb. Cross section near center of corallum x 3 

lc. Cross section near base of corallum x 3/4 
Wapanucka formation, station 28. 

LOPHOPHYLLUM PROFUNDUM Milne-Edwards and Haime 


Fig. 2. 

Specimen slightly above average size 

Boggy formation, station 169. 

?a. 

Specimen in which the walls of the calice are broken away so 
that the pseudocolumella is shown. 

Boggy formation, station 169. 


2b. and 2d. Cross sections x 3. 

Wetumka formation, station 161 


2c. 

Longitudinal section x 3. 

Wetumka formation, station 1661. 

Fig. 3 

LOPHOPHYLLUM PROFUNDUM RADICOSUM Girty 

and 3a. Two specimens rather above the average size. Fig. 3a 
shows the pseudocolumella. 

Wewoka formation, station 152. 


PLATE XXXII 














194 


PALEONTOLOGY 



THIS DESCRIPTION is for 

PLATE XXXV, PAGE 199 

PLATE XXXIII 

MICHELENIA EUGENEAE White 

Fig. 1. 

Cross section and longitudinal section x 3. 

Wapanucka formation, station 28. 

la. 

Top view of average size specimen. Natural size. 

Wapanucka formation, station 28. 

lb. 

Side view of a specimen from the Boggy formation, station 166 
x 1 V 2 . 

Fig. 2. 

MICHELENIA EXILIMURA Mather 

Cross section and longitudinal section x 3. 

Caney shale, station 170. 

Fig. 3. 

PACYPORA CANEYANA n. sp. 

Fragment of ccrallum showing average width. 

Caney shale, station 170. 

3 a. 

Cross section and tangential section x 3. 

Caney shale, station 170. 

Fi/ 4. 

MICHELENIA SUBCYLINDRICA Mather 

Longitudinal section and tangential section x 3Vs. 

Wapanucka formation, section 28 . 

4 a. 

Fragment of corallum. Natural size. 

Wapanucka formation, station 28. 


PLATE XXXIII 


























196 


PALEONTOIjOC V 


PLATE XXXIV 

TRIPLOPHYLLUM sp. 

Fig. 1. View from above of an average specimen. 

la. View from above of a specimen enlarged x 1^. 

lb. Cross seclion near top of corallum x 3. 

lc. Cross section near base of corallum x 3. 

id. Longitudinal section through center of corallum x 3. 

All specimens figured, from Wapanucka formation, station 28. 

Remarks: This is probably the form identified by Mather as Zaphrentis 

gibsoni. 


LONSDALEIA sp. 

Fig. 2. Cross section near top of corallum x 3. 

2a. Longitudinal section through central part of a fragment of coral¬ 
lum x 3. Specimens from Homer limestone member of the Hold- 
enville formation, station 197. 


PLATE XXXIV 











198 PALEONTOLOGY 

THIS DESCRiPTiC. jlS 

PLATE XXXU1. PAGE 193 

PLATE XXXV 

AGASSIZOCRINUS CON1CUS Owen and Shumard 
Fig. l. Side view of an average sized specimen. 

Wapanucka formation, station 28. 

CERIOCRINUS HEMISPHERICUS (Shumard) 

Fig. 2. Top view of calyx. Natural size. 

Boggy formation, station 166. 

CERIOCRINUS sp. (Probably a n. sp.) 

Fig. 3. Base of calyx. Natural size. 

3a. Side of calyx. Natural sizv. 

Both specimens from Wapanucka formation, station 23. 

EUPACHYCRINUS cf MAGISTER Miller and Gurley 
Figs. 4 and 4a. External surface of plates. Natural size. 

Wapanucka formation, station 28. 

HYDREIONOCRINUS sp. 

Figs. 5 and 5a. Brachial plates. Natural size. 

Boggy formation, station 169. 

PENTREMITES ANGUSTUS Hambach 
Fig. 6. Lateral view of a large specimen. Natural size. 

Wapanucka formation, station 28. 

PENTREMITES RUSTICUS Hambach 
Fig. 7. Lateral view of average specimen. Natural size. 

Wapanucka formation, station 28. 

STEREOBRACH1CRINUS PUSTULOSSUS Mather 
Fig. 8. A nearly complete arm. Natural size. 

Wapanucka formation, station 19. 

ARCHAEOCIDARIS AGASSIZI Hall 
Fig. 9. A well preserved plate, x \ V%. 

Boggy formation, station 98. 

ARCHAEOCIDARIS MEGASTYLUS Shumard 
Figs. 10 and 10a. Plate and stem, x \ Y%. 

Plate from Savanna formation, station 15. 

Stem from Francis formation, station 124. 

ARCHAEOCIDARIS sp. 

Fig. 11. Portion of a large spine, x i l A. 

Francis formation, station 124. 

Fig. lia. Cross section of spine. 

Remarks: This is probably a new species. The combination of arrange¬ 
ment of secondary spines, type of cross section and charac'er of 
base has not been observed in any described species. 


PLATE XXXV 
















200 


PALEONTOLOGY 


plat:: xxxvi 

ACANTHOCLEMA CARBONARIllM n. sp. 

Fig. 1. Longitudinal section x 18. Showing the median lamina and thick 
vestibules. 

Fig. 2. Tangential section x 18. 

CYSTODICTYA BRENTWOODENSIS Mather 
Fig. 3. Longitudinal section x 18. 

Fig. 4. Tangential section x 18. 

FENESTELLA MIMICA Ulrich 

Fig. 5. A splendid fragment of a zoarium reverse side x \ V\. 

FENESTELLA SEVILLENSIS Ulrich 

Fig., 6. A small fragment of a specimen showing the reverse, x 3^2. 
FENESTELLA cf. SEVILLENSIS 

Fig. 7. The reverse of a specimen x 3J4 more closely crowded filaments 
than F. sevillensis. 

FENESTELLA SPINULOSA Condra 
Fig. 8. A fragment of a large specimen x 1. 


PLATE XXXVI 





202 

Fig. 1. 
Fig. 2. 

Fig. 3. 
Fig. 4. 

Fig. 5. 

Fig. 6. 

Fig. 7. 
Fig. 8. 

Fig. 9. 

Fig. 10. 
Fig. 11. 

Fig. 12. 
Fig. 13. 

Fig. 14. 

Fig. 15. 
Fig. 16. 


PALEONTOLOGY 

PLATE XXXVII 

FENESTELLA VENliSTA Mather 
Reverse of a zoarium x 3^2. 

FISTULIPORA SUTILIS n. sp. 

A splendid zoarial fragment x 1%. 

(See Plate x figs, l, 2) 

GLYPTOPORA CRASSISTOMA Mather 
Tangential section x 18 showing wide interspaces filled with num¬ 
erous crysts. 

Longitudinal section x 18. 

GLYPTOPORA INCRUSTANS n. sp. 

A fragment of a zoarium incrusting a crinoid stem, x 3J4. 
GLYPTOPORA STONEWALLENS1S n. sp. 

A portion of the zoarium x 3^ “dimple” maculae and zooecia 
distribution. 

POLYPORA CESTRIENSIS Ulrich 
A portion of the zoarium x \ Vs showing reverse side. 

POLYPORA CRASSA Ulrich 

A fragment of the zoarium showing the distribution of the zooecial 
openings, x 3 . 

POLYPORA ELLIPTICA Roge:s 
A portion of a poorly preserved zoarium showing porous surface, 
x 3 

POLYPORA NODOCARINATA Ulrich 
A splendid f agment of the porous surface, x 3J4. 

POLYPORA SPINULIFTR A Ulrich 
Porus surface of fragment, x 3J4. 

POLYPORA WHITEI Ulnch 
The reverse side of a well preserved fragment, x 3J4. 

POLYPORA WHITEI 1NSCULPTA Ulrich 
A view of a partially covered obverse surface, x 3 Vi. 

RHOMBOPORA SNIDERI Mather 
Portion cf a zoarium x 3 showing the characteristic branch¬ 
ing. 

SEPTOPORA BISER1AL1S (Swallow) 

A fragment of the porous surface x 3^. 

SEPTOPORA CESTRIENSIS Prout. 

A portion of the porous side of the zoarium x 3 l z. 


PLATE XXXVII 







204 


PALEONTOLOGY 


Fig. 1, 
Fig. 2 

Fig. 3, 
Fig. 4 
Fig. 5, 

Fig 6. 
Fig. 7. 

Fig. 8. 
Fig. 9. 
Fig. 10. 







PLATE XXXVIII 

FISTULIPORA SUTILIS n. sp. 

Tangential section x 18. 

Longitudinal section x 18 showing the bilaminate structure. 

RHOMBOPORA LEPIDODENDROIDES Meek 
A fragment of zoarium x 3 Vi. 

Tangential section x 18. 

Longitudinal section x 18. 

RHOMBOPORA PERSIMILIS Ulrich 
Longitudinal section x 18 showing numerous central tubes. 
Tangential section x 18 cut slightly deep. 

RHOMBOPORA SUBCRASSA n. sp. 

A fragment of a zoarium x 3 I / 2 . 

Longitudinal section x 18. 

Tangential section x 18 showing large acanihopores among the 
numerous dark spots. 


PLATE XXXVIII 




r**; * 


•<v 


‘ :?-.v 







206 


PALEONTOLOGY 



PLATE XXXIX 

SEPTOPORA ROBUSTA Ulrich 

i. • - 

Fig. l. Fragment of a zoarium x 3 showing porous side. 

STENOPORA BOGGYENSIS n. sp. 

Fig. 2. A portion of zoarium x 1^4. 

Fig. 3. Tangential section x 18. 

Fig. 4. Longitudinal section x 18 showing a few of the axial thicken¬ 
ings. 

STENOPORA BULLATA n. sp. 

Fig. 5. Longitudinal section x 18 showing the numerous small beads 
and large acanthopores. 

Fig. 6 Tangential section x 18. 

STENOPORA CARBONARIA (Worthen) 

Fig. 7. Longitudinal section x 18. 

Fig. 8. Tangential section x 18. 

STENOPORA CARBONARIA CONFERTA Ulrich 

Fig. 9. Longitudinal section x 18. 

(See Plate XL, fig. l.) 


PLATE XXXIX 





> \ . 1 


PLATE XL 

STENOPORA CARBONARIA CONFER! A Lilrich 

Fig. 1. Tangential section x 18 showing very large acanthopores. 

(See Plate XI Fig. 9.) 

STENOPORA CIRCINA n. sp. 

Fig. 2. A portion of a zoarium x 

Fig. 3. Tangential section x 18 with several mesopores showing. 

Fig. 4. Longitudinal section x 18. 

STENOPORA HETEROPORA Condra 
Fig. 5. A tangential section x 18. 

STENOPORA MACALESTERANA n. sp. 

Fig. 6. A longitudinal of the mature and submature region x IS. 

Fig. 7. A portion of a zoarium x 1 24 

(See Plate XLI, fig. 3.) 


PLATE XL 






JWj &WfBk f fr 



W%mM 

pjjjpfeijl yaja * 


Sfc^ y 1 

ft 'JPSSf * 

Mdc* I ^j||K 


ijy. 

T§fJ|? n|n 

,J f .+ ;|f * ap*B 

tw. 


W,' *** ?**' 1 

j| 


g||< 

; W ijpl 

if 

wm\ "V, a 

Ljlfi 

, Jjfak Ja > • 

jap : jp% * Jm»g 

V 


\ 






210 


Fig. 1. 
Fig. 2 

Fig. 3 

Fig. 4 
Fig. 5 

Fig. 6 
Fig. 7 

Fig. 8 
Fig. 7. 


PALEONTOLOG7 


PLATE XLI 

STENOPORA HIPSIDA n. sp. 

Longitudinal se:tion x 18 showing numerous perforated diaph¬ 
ragms. 

Tangential section x 18 showing he numerous acanthopores. 

STENOPORA MACALESTERANA n. sp. 

Tangential section x 18 showing the variable wall thickness. 

STENOPORA MICROPORA n. sp. 

Tangential section x 18 showing the numerous mesopores. 
Longitudinal section x 18. 

STENOPORA TUBERCULATA (Prout) 

Fragment ot zoaiium x 1 %. 

Tangential section x 18. 

STENOPORA WAPANUCKAENS1S n. sp. 

Tangential section x 18. 

Longitudinal section x 18 showing the extensive thickenings. 


PLATE XLI 






mm. 





212 


PALEONTOLOU V 


Fig. 


PLATE XLII 

AMBOCOELIA PLANOCONVEXA (Shumard) 

1. A broad specimen without sinus, 
la. Dorsal view. 

Boggy formation, station 166. 


ATHYRIS sp. 

Fig. 2 . Cast of the only specimen obtained. 

Wewoka formation, station 76. 

AULACORHYNCHUS MILLEPUNCTATUS (Meek and Worthen) 

Fig. 3. Fragment of ventral valve. 

Francis formation, station 198. 

CHONETES GRANULIFER Owen 

Figs 4. and 4b. Ventral views. 4a. Dorsal view. 

Francis formation, station 124. 

CHONETES GRANULIFER ARMATUS Girty 

Fig- 5. Ventral view of a small specimen with well preserved spines x 2 . 
After Girty U. S. G. S. Bull. 544, 

Fauna of the Wewoka formation. 

CHONETES MESO'LOBUS Norwood and Pratten 

Figs. 6 and 6a. Ventral views of average sized specimens. 

Wewoka formation, station 152. 


CHONETES MESOLOBLS DECIPIENS Girty 

Fig. 7. Ventral view, after Girty U. S. G. S.; Bull. 544 , 
Fauna of the Wewoka formation. 


PLATE XLII 



wJmM 












214 


PALEONTOLOGY 


PLATE XLII—Continued 

CHONETES MESOLOBUS EUAMPYGUS Girty 

Fig. 8. Ventral view of a rather larg£ specimen after Girty, U. S (i > 
Bull. 544, 

Fauna of the Wewoka formation. 

CHONETES PLANUMBONUS CHOCTAWENSIS Girty 
Fig. 9. Ventral view. 

Upper part of Woodford formation, station 74. 

CLEIOTHYRIDINA ORBICULARIS* (McChesney) 

Fig. 10. Ventral view. 

Wewoka formation, station 130. 

10a. Dorsal view of small specimen. 

Holdenville formation, station 232. 

10b. Ventral view of a large individual after Girty, U. S. G. S. Bull 
544, 

Fauna of the Wewoka formation. 

COMPOSITA GIBBOSA Mather 

Fig. 11. Dorsal view. 

Wapanucka formation, station 23. 

COMPOSITA OZARKANA ? Mather 

Fig. 12. Lateral view of an individual doubtfully assigned to this species. 
Wapanucka formation, station 23. 

COMPOSITA SUBTILITA (Hall) 

Fig. 13. Lateral view. 

13a. Ventral view. 

Sasakwa limestone member of the Holdenville formation, static” 
230. 


PALEONTOLOGY 


215 


PLATE XLII—Continued 

COMPOSITA WASATCHENSIS (White) 
figs. 14-1 5a. Ventral views cf two specimens referred to this species. 7/ap 



anucka formation, station 28. 

Fig. 15. 

CRANIA MODESTA White and St. John 

Individual cf average size attached to Spi:ifer cameratus. Boggy 
iormation, station 169. 

Fig. 16. 

DERBYA CRASSA (Meek and Hayden) 

Dorsal view. 16a. Ventral view. Boggy formation, Station it. 

Fig. 17. 

DIELASMA ARKANSANUM Weller 

Ventral view. McAlester formation, station 52. 

Fig. 18. 

DIELASMA BOVIDENS Morton 

Dorsal view of cast, above average size. Wewoka formation, sta¬ 
tion 130. 

Fig. 19. 

DIELASMA SUBSPATULATUM Weller 

Ventral view of broken pedical valve. Wapanucka formation, sta¬ 
tion 23. 


19a. Ventral view of cast. Atoka formation, station 58. 


Fig. 20. 

ENNTELETES HEMIPLICATA (Hall) 

Ventral view x 3%. 20a. Ventral view x 2%. Homer limestone 

member, Holdenville formation, station 216. 


HARTTINA BREVILOBATA (Swallow) 


Fig. 21. Dorsal view. Top of Woodford formation, station 74. 


PALEONTOLOGY 


216 


Figs. 

Fig. 

Figs. 

Fig- 

Fig. 

Fig. 

Fig- 

Fig. 

Fig- 

Fig. 

Figs. 

Figs. 

Fig. 

Fig. 

Fig. 

Fig. 

Fig. 

Fig- 

Fig. 


PLATE XLIII 

HUSTEDIA BRENTWOODENSIS Mather 
l and la. Dorsal and lateral views. Wapanucka formation, station 41. 
HUSTEDIA MISERI Mather 

2. and 2a. Dorsal and ventral views. Wapanucka formation, station 
28 . 

HUSTEDIA MORMONI Marcou 
3 and 3a. Ventral views. Boggy formation, station 98. 

LINGULA BATESVILLAE Girty 

4. Ventral valve. Top Woodford formation, station 64. 

LINGULA PARACLETUS Hall and Clark 

5. Ventral valve, compressed. Top Woodford formation, station 64. 

LINGULA UMBONATA Cox 

6. Fragment of ventral valve. Boggy formation, station 169. 

LINGULODISCINA NEWBERRYI CANEYANA Girty 

7. Ventral valve x 3. Caney shale, station 63. 

LIORHYNCHUS CARBONIFERUM Girty 

8. Cast of dorsal valve. Top of Woodford formation, station 64. 
LIORHYNCHUS CARBONIFERUS POLYPLEURUM Girty 

9. Dorsal valve. Top of Woodford formation, station 64. 

LINGLIPORA NEBRASKENSIS (Meek) 

10. Exterior of a very good specimen. Boggy formation, station 169. 

MARGINIFERA MURICITA (Norwood and Patten) 

11 and lla. Ventral and lateral views. Wewoka formation, station 
152. 

MARGINIFERA SPLENDENS (Norwood and Patten) 

12 and 12a. Ventral and dorsal views. Wewoka formation, station 
152. 

MARTINIA n. sp. 

13. Ventral view showing sinus. Identification by Professor Charles 
Schuchert. Sycamore limestone, station 73. 

MARTINIA GLABRA Martin 

14. Ventral view. Top Woodford formation, station 74. 

MEEKELLA STRIATACOSTATA Cox 

15. Wax cast of ventral valve. Belle City limestone, Station 184. 

ORBICULOIDEA CONVEXA (Shumard) 

16. Dorsal valve viewed from above. McAlester formation, Station 52. 

PRODUCTELLA HIRSUTIFORMIS Walcott 

17. Crushed, ventral valve. Top Woodford, formation, station 64. 

PRODUCTUS CORA D’Orbigny 

18. Ventral valve. Wetumka shale, station 161. 

PRODUCTUS GALLITINSIS Girty 

19. Ventral valve viewed from above. Wapanucka formation, Station 
37. 


PLATE XLIII 









218 


PALEONTOLOGY 


Fig- 

Fig- 

Fig- 

Figs. 

Fig. 

Fig. 

Figs. 

Fig. 

Fig. 

Fig. 

Fig. 

Fig- 

Fig- 

Fig. 


PLATE XLIV 

PRODUCTUS GALLOWAYI n. sp. 

l Ventral view, showing fold and medial spines, 
la. Lateral view showing projecting beak and wrinkles on ears. Both 
specimens from Wapanucka formation, station 3 7. 

PRODUCTUS 1NSINUATUS Girty 

2. Ventral view showing fold. Wewoka formation, station 201. 

PRODUCTUS MORROWENSIS Mather 

3. Lateral view. 3a. Ventral view. Wapanucka formation, station 
23. 

PRODUCTUS NANUS Meek and Worthen 
4 and 4a. Ventral and lateral views. Wapanucka formation, station 23. 

PRODUCTUS PERTENUIS Meek. 

5. Ventral valve viewed from above. Seminole formation, station 62. 

PRODUCTUS SEMIRETICULATUS Martin 

6. Ventral view, Wewoka formation, station 130. 

PUGNAX OSAGENSIS (Swallow) 

7. 7a, 7b, 7c. Top, dorsal, ventral and basal views. Boggy formation, 

station 166. 

PUGNAX ROCKYMONTANA (Marcou) 

8. Dorsal view. Wetumka formation, station 163. 

PUSTULA BULLATA (Mather) 

9 and 9a. Ventral and lateral views. Wapanucka formation, station 23. 
PUSTULA NEBRASKENSIS (Owen) 

10. A very good specimen from the Wewoka formation, Station 156. 

PUSTULA PUNCTATA (Martin) 

11. Fragment of a very large individual. Wewoka formation, station 
130. 

PUSTULA SUBLINEATA Mather 

12. Ventral valve viewed from above. Top of Caney formation, sta¬ 
tion 170. 

RHYNCHOPORA ILLINOISENSIS (Worthen) 

13. Fragment of ventral valve. Francis formation, station 124. 

RHYNCHOPORA MAGNICOSTA Mather' 

14. Dorsal view. Wapanucka formation, station 170 A. 


PLATE XLIV 











220 


PALEONTOLOGY 


PLATE XLV 

ROEMERELLA PATULA Girty 

Fig. 1. Dorsal valve of unusually large specimen. 

la. Ventral valve of specimen of average size. Boggy formation, sta¬ 
tion 166. 

SCHIZOPHORIA RESUPINOIDES Cox 

Fig. 2. Interior of brachial valve. 

2a. Exterior of brachial valve. Wapanucka formation, station 3 7. 

SPIRIFER CAMERATUS Morton 

Fig. 3. Ventral valve. 

3a. Cardinal area. Both specimens from Boggy formation, station 
169. 

SPIRIFER GOREII Mather 


Fig. 4. Ventral view. 

4a. Dorsal view. Anterior portion of both specimens somewhat broken 
away. Wapanucka formation, station 28. 

SPIRIFER OPIMUS Hall 

Figs. 5 and 5a. Ventral valves. McAlester formation, station 50. 
SPIRIFER ROCKYMONTANUS Marcou 


Fig. 6. Ventral valve. Boggy formation, station 12. 

6a. and 6b. Dorsal and lateral views of a small specimen Boggy for¬ 
mation, station 169. 

SPIRIFERINA CAMPESTRIS White 


Fig. 7. Ventral valve. Wapanucka formation, station 28. 

7a. Ventral valve, x 2. Wapanucka formation, station 28. 

SPIRIFERINA KENTUCKYENSIS Shumard 


Fig. 8. Ventral valve of a very good specimen x 3%. 

Boggy formation, station 169. 

SPIRIFERINA TRANSVERSA (McChesney) 

Fig. 9. Brachial valve. Wapanucka formation, station 28. 

SQUAMULARIA PERPLEXA (McChesney) 

Fig. 10, 10a, and 10b. Lateral, ventral and cardinal views. Boggy forma¬ 
tion, station 165. 


PLATE XLV 









222 


PALEONTOLOGY 


Fig. 

Fig- 


Fig. 

Fig. 

Fig. 

Fig- 

Fig. 

Fig. 

Fig- 

Fig- 

Fig- 

Fig. 

Fig. 

Fig- 


Fig. 


PLATE XLVI 

ACANTHOPECTEN CARBONIFEROUS (Stevens) 

1. Impression of left valve. Francis formation, Station 124. 

la. Impression of left valve after Girty, U. S. G. S. Bull. 544, Fauna 
of the Wewoka formation. 

ALLORISMA? n. sp. 

2. Left valve and partial view of cardinal area. Wetumka formation, 
station 161. 

Remarks: —In this specimen, and in several others, obtained, the 
concentric striations alternate in the sinus near the base of the 
shell. This characteristic, however, is not constant; sometimes it 
is not shown at all ana often it is present on only one vaive, 
either right or left. No description has been found in the litera¬ 
ture and the shell is thought to be a new species. 

ALLORISMA TERMINALE Hall 

3. Internal mold of specimen of average size. 

3a. Broken internal mold viewed from above. Boggy formation, sta¬ 
tion 13 5. 

ANTHROCONEILO TAFFIANA Girty 

4. Left valve. 

4a. Cardinal area. Boggy formation, station 166. 

ASTARTELLA CONCENTRICA McChesney 

5. Left valve. Boggy formation, station 166. 

ASTARTELLA VARICA McChesney 

6. Right valve. Senora formation, station 163. 

AVICULOPECTEN ARKANSANUS Mather 

7. An impression of a left valve. McAlester formation, station 52. 

AVICULOPECTEN OCCIDENTAL1S (Shumard) 

8. An impression of what is thought to be a right valve. Francis 
formation, station 124. 

AVICULOPINNA AMERICANA Meek 

9. Fragment of a right valve. Wetumka formation, station 163. 

CANEYELLA RICHARDSONI Girty 

10. Impression of right valve. Caney formation, station 150. 

CANEYELLA VAUGHNI Girty 

11. Impression of right valve. Caney formation, station 150. 

CANEYELLA WAPANUCKENSIS 

12. Right valve, larger than those figured by Girty. Caney forma¬ 
tion, station 150. 

CONOCARDIUM SNIDERI n. sp. 

13. Right valve of cotype. 

13a. Basal view of cotype, showing gaping and crenulate edges of 
valves. 

13b. Front view of cotype. Caney formation, station 170. 

CONOCARDIUM OBLIQUUM Meek and Worthen 

14. Right valve. Boggy formation, station 12. 


PLATE XLVI 








224 


PALEONTOLOGY 


Hg. 

Fig- 

Figs. 

Fig. 

Fig- 

Fig. 

Fig. 

Fig. 

Fig. 

Fig- 

Fig. 

Fig. 


Fig. 

Fig- 

Fig. 

Fig. 


PLATE XLVII 

CYPRICARDIN1A CARBONARIA Meek 

1. Left valve. Francis formation, station 124. 

DELTOPECTEN TEXANUS Girty 

2. Fragment of specimen of average size. Boggy formation, station 

169. 

EDMONDIA sp. 

3 and 3a. Two right valves referred to this genus. Boggy formation, 
station 169. 

EDMONDIA ASPINWALLENSIS Meek 

4. A right valve. Wewoka formation, station 13 0. 

EDMONDIA? NEBRASKENSIS (Geinitz) 

5. Fragment doubtfully referred to this species. McAlester forma¬ 
tion, station 7. 

EDMONDIA? REFLEXA Meek 

6. A rather poorly preserved specimen. Boggy formation, station 
91. 

LEDA BELLISTRIATA Stevens 

7. Right valve. Savanna formation, station 47. 

7a. Cardinal area. Wewoka formation, station 203. 

LEDA BELLISTRIATA ATTENUATA (Meek) 

8. Left valve, Senora formation, station 158. 

LEDA sp. 

9. A large individual with a tendency toward grouping of the slriae, 
four or five bounded on either side by a pronounced growth line. 
Holdenville formation, station 232. 

LIMA RETIFERA Shumard 

10. An almost perfect left valve. Holdenville formation, station 202. 

MODIOLA SUBELLIPTICA Meek? 

11. Left valve. Boggy formation, station 166. 

MYALINA sp. • 

13. Left valve of what is probably a new species. Except for its 
greater size, however, this form is very close to M. swallowi Mc- 
Chesney and for that reason is not described as new. Boggy for¬ 
mation, station 9l. 

MYALINA SUBQUADRATA (Shumard) 

12. Left valve, Francis formation, station 228. 

MYALINA SWALLOVI (McChesney) 

14. Right valve. Boggy formation, station 11. 

NUCULA ANONDONTOIDES (Meek) 

15. Left valve. l5a. Cardinal area, Boggy formation, station 100. 

NUCULA PARVA (McChesney) 

16. Right valve. Wapanucka formation, station 41. 


PLATE XLVII 











PALEONTOLOGY 

XLVII—Continued 

NUCULOPSIS VENTRICOSA (Hall) 

Right valve. 17a. Anterior view. 17b. Cardinal view. We 
woka formation, station 203. 

PARALLEDON OBSOLETUS (Meek) 

Left valve, Francis formation, station 124. 

PARALLEDON SANGAMONENSIS (Worthen) 

Internal mold of left valve. Boggy formation, station 87. 
PARALLEDON TENUISTRIATUS (Meek and Worthen) 

Fragment of left valve. McAlester formation, station 8. 

PINNA PERACUTA Shumard 

Internal mold of right valve. Top bed of Wewoka formati<>-\ 
station 76. 


PLATE XLVIII 

PLEUROPHOROUS cf. SUBCOSTATUS Meek and Worthen 
Fig. l. Left valve. Wetumka formation, station 163. 

PLEUROPHOROUS TROPIDOPHOROUS Meek 
Fig. 2. Internal mold of right valve. Boggy formation, station 98. 

POSODONIA VINTONENSIS Morningstar 
Fig. 3. Right valve. Seminole formation, station 62. 

PSEUDOMONOTIS HAWNI Meek and Hayden 
Fig. 4. Fragment of large right valve. Holdenville formation, station 7 7. 

PTERIA LONGA (Geinitz) 

Fig. S. Left valve. Holdenville formation, station 215. 

SCHIZODLS AFFINIS Herrick 

Fig. 6. Internal mold of right valve. Wewoka formation, station 76 

SCHIZODUS ALPINUS (Hall) 

Fig. 7. Left valve. 7a. Anterior view. Wewoka formation, station 203. 

SCHIZODUS AMPLUS Meek and Worthen 
Fig. 8. Fragment of right valve. Wapanucka formation, station 28. 

SCHIZODUS aff. MEEKANUS 

Fig. 9. Fragment of large left valve. McAlester formation, station Si. 

9a. Left valve of small specimen doubtfully referred to this species. 
Boggy formation, station 169. 

SCHIZODUS sp. 

Fig. 10. Left valve of what is probably a new species. McAlester forma¬ 
tion, station 48. 

YOLDIA GLABRA 

Figs. 11 and lla. Left valves. Boggy formation, station 166. 


226 

Fig. 17. 

Fig. 18. 
Fig. 19. 
Fig. 20. 
Fig. 21. 


PLATE XLVII1 







228 


PALEONTOLOGY 


Fig. 

Fig- 


1 . 


2 . 


Fig. 3. 


Fig. 

4. 

Fig. 

5. 

Fig- 

6. 

Fig. 

7. 

Fig. 

8. 

Fig- 

8. 

Fig. 

10. 

Fig. 

1 1 . 

Fig. 

12. 


Fig- 

12b 

PA 

Fig. 

13. 

P 

Fig. 

14. 

Fig- 

15. 

Fig. 

16. 

Fig- 

17. 

Fig. 

18. 


PLATE XLIX 

BELLEROPHON BELLUS Keyes 
Dorsal view. Ada formation, station 209a. 

BELLEROPHON CRASSUS Meek and Worthen 
Dorsal view of a very large specimen. McAlester formation, 
station 17. 

BELLEROPHON CRASSUS WEWOKANUS Girty 
Side view. Holdenville formation, station 79. 

Remarks: —B. crassus wewokanus is distinguished from B. crassus 
by the form of the umbilicus. In the latter it is open while in 
the former it is closed. 

BELLEROPHON MARCOUANUS Geinitz 
Dorsal view. Wetumka formation, station 163. 

BUCANOPSIS MEEKIANA (Swallow) 

Dorsal view. Boggy formation, station 166. 

EUOMPHALUS sp. 

Side view. Caney formation, s ation 3 3. 

EUPHEMUS CARBONARIUS (Cox) 

Side view. 7a. Dorsal view, Boggy formation, station 96. 

EUPHEMUS NODOCARINATUS (Hall) 

Apertural view. Holdenville formation, station 79. 

MEEKOSPIRA PERACUTA CHOCTAWENSIS Girty 
Apertural view. 9a. Side view of a cracked and broken speci¬ 
men. Wetumka formation, station 161. 

MURCHISONIA TEREBRA White 
A broken specimen. Savanna formation, station 47. 

NATICOPSIS ALTONENSIS (McChesney) 

Side view. lla. Top view. Holdenville formation, station 79. 

NATICOPSIS REMEX (White) 

Top view of cast. Belle City formation, station 225. 

12a. Side view cf a somewhat crushed cast. Holdenville formation, 
station 230. 

NATICOPSIS SUBOVATUS Meek and Worthen 
12b. Side view Francis formation, station 124. 

PATELLOSTIUM MONTFORTIANUM (Norwood and Pratten) 

Dorsal view. 13a. Side view. Wewoka formation, station 205. 
PHANEROTREMA GRAYVILLENSE (Norwood and Pratten) 

Side view. 14a. Top view. Caney formation, station 33. 

PHARKIDONOTUS PERCARINATUS (Conrad) 

Dorsal view. l5a. Side view. Holdenville formation, station 7 7. 

PLATYCERAS PARVUM (Swallow) 

Side view. Boggy formation, station 93. 

PLEUROTOMARIA ARENARIA Girty 
Side view. Vanoss formation, station 209a. 

PLEUROTOMARIA BROADHEADI White 
Top view of a crushed cast. Francis formation, station 124. 


PLATE XLVIX 



■ 











230 


PALEONTOLOGY 


Fig. 

19. 

Fig. 

20. 

Fig. 

21. 

Fig. 

22. 

Fig. 

23. 

Fig. 

1 . 

Fig. 

2. 

Fig. 

3. 

Fig. 

4. 

Fig. 

5. 


5a. 

Fig- 

6. 

Fig. 

7. 

Fig. 

8. 

Fig. 

9. 

Fig. 

10. 

Fig. 

11 . 

Fig. 

12. 

Fig. 

13. 


13a 


Fig. 14. 


XLIX—Continued 

PLEUROTOMARIA MISSOURIENSIS (Swallow) 

Side view of a broken specimen. Wapanucka formation, station 

28 . 

PLEUROTOMARIA MONILIEERA (White) 

Top view. Savanna formation, station 44. 

PLEUROTOMARIA PERHUMEROSA Meek 
Side view. Wetumka formation, station 163. 

PLEUROTOMARIA SPIRONEMA Meek ar.d Worthen 
Top view. Holdenville formation, station 230. 

PLEURTOMARIA SUBCARBON ARIA Keyes 
Top view. Boggy formation, station 169. 

PLATE L 

PLEUROTOMARIA TAGGERTI Meek 
Side view of a broken cast. Francis formation, station 228. 

SCHIZOSTOMA CATILLOIDES (Conrad) 

Side view. Boggy formation, station 169. 

SCHIZOSTOMA SUBQUADRATUS (Meek and Worthen) 

Side view of a worn specimen. Francis formation, station 228. 

SOLENISCUS FUSIFORMIS (Hall) 

Apertural view. Wewoka formation, station 13 0. 

SPHAERODOMA BREVIS (While) 

Side view. Wetumka formation, station 163. 

Apertural view. Boggy formation, station 1 71. 

SPHAERODOMA GRACILIS (Cox) 

Side view of cast. Boggy formation, station 7 5. 

SPHAERODOMA INTERCALCARIS (Meek and Worthen) 

Side view, Wetumka formation, station 161. 

SPHAERODOMA PONDEROSA (Swallow) 

Side view. Belle City formation, station 225. 

SPHAERODOMA PRIMIGENIA (Conrad) 

Apertural view. Belle City formation, station 225. 

STROPHOSTYLUS NANA (Meek and Worthen) 

Top view. Francis formation, station 228. 

TRACHYDOMIA WHEELERI (Swallow) 

Top view of average specimen, lla. Side view of a large speci¬ 
men. Holdenville formation, station 79. 

TREPOSPIRA DEPRESSA (Cox) 

Top view. Boggy formation, station 161. 

WORTHENIA TABULATA Conrad 
Side view of a very large specimen. 

Top view of specimen of average size. Francis formation, sta'ion 

124. 

CONULARIA CRUSTULA White 
Side view. Senora formation, station 158. 


PLATE L 










232 


PALEONTOLOGY 


' s/# . 

ifl 


PLATE LI 


ACTINOCERAS VAUGHAIANUM Girty 

Fig. 1. Side view of a worn specimen. Caney formation, station 63. 

ADELPHOCERAS MESLERIANUM .Girty 

Fig. 2. Side view. Caney formation, station 150. 

BACRITES (?) QUADRILINEATllS Girty 

Fig. 3. Base, showing marginal siphuncle. 3a. Side view Caney fo mo¬ 
tion, station 150. 

COLOCERAS LIRATUM Girty 

Fig. 4. Side view. 4a. Ventral view showing simple sutures. Boggy 
formation, station 165. 

CYRTOCERAS sp. 

Fig. 5. Side view of large specimen. 

5a. Cross section of smaller spe:imen. Wewoka formation, station 


130. 


DIMORPHOCERAS TEXANUM Smith 


Fig. 6. 

Fig. 

Fig. 

Fig. 

Fig. 


Side view of fragment showing sutures and umbilicus. Wewoka 
formation, station 204. 

EPHIPPIOCERAS FERRATUS (Cox) 

7. Ventral view showing simple sutures. Francis formation, sta ion 

228 . 

GASTRIOCERAS ANGULATUM Girty 

8. Dorsal view. 8a. Side view. Boggy formation, station 166. 

GASTRIOCERAS EXCELSUM (Meek) 

9. Fragment of venter showing characteristic sutures. Wewoka for¬ 
mation, station 130. 

GASTRIOCERAS HYATTIANUM .Girty 

10. Ventral view showing sutures. Wewoka formation, station 152. 
10a. Side view, showing umbilicus. Wewoka formation, station 15 6. 


PLATE LI 











234 


PALEONTOLOGY 


PLATE LII 


Fig. 1. 

la. 

GASTRIOCERAS KANSASENSE (Miller and Gurley) 

Dorsal view of small specimen. 

Side view of larger specimen. Caney formation, station 170. 

Fig. 2. 

GASTRIOCERAS L1STERI (Martin) 

Fragment showing nodes along side of whorl. Caney formation, 
170. 

Remarks. —At this locality G. listeri is very abundant. Several 
specimens were collected with diameters of more than two 
inches. 

Fig. 3. 

GONIATITES CHOCTAWENSIS (Shumard) 

Side view. 3a. Forsal view. Caney formation, station 144. 

Fig. 4. 

1DIOTHECA RUGOSA Girty 

An impression. This form is thought to be a portion of an aptycus 
or operculum of a cephalopod. Woodford formation, station 146. 

Fig. 5. 

GONIOLOBOCERAS WELLERI Smith 

Fragment showing sutures. Wewoka formation, station 205. 

Fig. 6. 

GONIOLOBOCERAS WELLERI GRACILE Girty 

Fragment showing sutures. Wetumka formation, station 161. 

Fig. 7. 

7a. 

DRYOCHOCERAS BRAINERDI n sp. 

Lateral view. 

Suture 

7b. 

Apertural view. 

Canev formation, station 14Q* 


PLATE LIJ 












236 PALEONTOLOGY 

PLATE LIII 

METACOCERAS CORNUTUM Girty 
Fig. l. Ventral view of fragment. Boggy formation, station 166. 
la. Side view of fragment. Francis formation, station 124. 

ORTHOCERAS CANEYANUM Girty 

Fig. 2. Side view showing area of surface ornamentation. Caney forma¬ 
tion, station 150. 

ORTHOCERAS TliBA Girty 

Fig. 3. Side view of crushed specimen. Wetumka formation, station 206. 

ORTHOCERAS WAPANUCKENSE Girty 
Fig. 4. Side view. Caney formation, station 141. 

PROBELOCERAS? LUTHER1 Clark 

Fig 5 Side view of a very poorly preserved specimen doubtfully refer¬ 
red to this genus and species. Woodford formation, station 8A. 
Remarks: —Although sutures are not preserved on this specimen, 
its general appearance is so close to similarly crushed forms of 
Probeloceras from the Portage that the identification here given 
is thought to be very probably correct. 

PROTOCYCLOCERAS? RUSHENSE (McChesney) 

Fig. 6. Side view. Boggy formation, station 166. 

PSEUDORTHOCERAS KNOXENSE (McChesney) 

Fig. 7. Side view. Boggy formation, station 966. 

SCHISTOCERAS FULTONENSE (Miller and Gurley) 

Fig. 8. Apertuptfl view. 4 *. Side vi$*v. Belle CUy formation, s*5.ion 225. 

SCHISTOCERAS J*ULTONDKSE 
Fig. 8. Apertural view. 

Sa. Side view. 

Belle City formation, station 225. 

GRIFFITHIDES MORROWENSIS Mather 

Fig. 9. Fragment of cephalon. 9a. Fragment of pygidium. Wapanucka 
formation, station 23. 

GRIFFITHIDES PARVULUS Girty 

0ig- 10. Cephalon and part of thorax of a well preserved specimen. Bog¬ 
gy formation, station 169. 

PHILLIPSIA SANGAMONENSIS (Meek and Worthen) 

Fig. ll. Pygidium. Francis formation, station 124. 


PLATE LIII 



(\ fill 


j A 4 

%yj 













238 


PALEONTOLOGY 


PLATE LIII—Continued 

CLADODUS AlORTIFER (Newberry and Woithen) 
lig 12. Anterior face, Boggy formation, station 93. 

PETALODUS DESTRUCTOR (Newberry and Worthen) 
Tig. 13. Anterior face. Francis formation, station 124. 

PETRODUS OCCIDENTALS (Newberry and Worthen) 
Fig 14. Top view. Boggy formation, station 1669 . 


REGISTER OF LOCALITIES 


239 


REGISTER OF LOCALITIES 

4. Sandstone outcrop in road 54 mile south of the NE. cor., sec. 1, T. l N., 

R. 6 E. McAlester formation. 

5. Limey sandstone 30 feet south of locality four. McAlester formation. 

6. Limestone in creek bed at base of steep bluff 1,200 feet southeast of 

locality four. McAlester-Caney contact. 

7. Limestone (same as at 6) in creek bed northwest of center of sec. 1, T. 

1 N., R. 6 E. McAlester-Caney contact. 

8. North bank of creek north of center of sec. 1, T. l N., R. 6 E. McAlester 

formation. 

8a. In road SE. cor., sec. 1, T. 1 N., R. 6 E. Woodford formation near base. 

11. In gully 900 feet north of center or sec. 4, T. 1 N., R. 7 E. Boggy forma¬ 

tion, lower part. 

12. Shale bed west of Canyon Creek, 1,600 feet east and 650 feet north of the 

SE. cor., of sec. 4, T. 1 N., R. 7 E. Boggy formation, lower part. 

13. Shale in road, south of house NE. 54 sec. 5, T. 1 N., R. 7 E. Boggy for¬ 

mation, lower part. 

14. In shale, 1,800 feet east and 800 feet south of the NE. cor., of sec. 5, 

T. 1 N., R. 7 E. Boggy formation, lower part. 

15. Shale bed, northeast of J. S. Jolly’s house south central part of sec. 5, 

T. 1 N., R. 7 E. Savanna formation, upper part of exposed portion. 

16. Shale, south bank of creek 250 feet east of road in west central part of 

sec. 6, T. 1 N., R. 7 E. MsAlester formation, upper part. 

17. Red limestone, 400 feet northeast of SW. cor. of NW. 54 > section 6, T. 

1 N., R. 7 E. This is the limestone that, in the eastern part of the 
quadrangle, occurs 15 feet below the Lehigh coal of the McAlester 
formation. 

18. Conglomerate, 1,300 feet east and 1,800 feet north of the SW. cor., 

sec. 6, T. 1 N., R. 7 E. McAlester formation, upper part. (Base here 
overlapped.) 

19. Shale with thin beds of limestone, 900 feet north and, 200 feet east of 

the SW. cor. of SE. 54 , sec. 6, T. 1 N., R. 7 E. Wapanucka forma¬ 
tion, lower part. 

20. Limestone, secs. 5, 8, 9, 10, and 11, T. 1 N., R. 7 E. Boggy formation, 

near base. 

22. Limestone, 1,450 feet south and 1,300 feet west of the NE. cor., sec. 8, 

T. 1 N., R. 7 E. Savanna formation, upper part. fe 

23. Limestone, Canyon Creek in east central part of section 8, T. 1 N., R. 

7 E. Wapanucka formation, upper part. 

28. Limestone and shale, 900 feet north of SE. cor., sec. 8, T. 1 N., R. 7 E. 
Wapanucka formation, near base. 

33. Thin impure limestone, 250 feet north of the SE. cor., sec. 8, T. 1 N., 
R. 7 E. Caney shale, near top. 


240 


REGISTER OF LOCALITIES 


36. Shale, bed of Canyon Creek southeast of the center of sec. 8, T. 1 M., 
R. 7 E. Caney shale, upper part. 

3 7. Shale, bed of Canyon Creek, east central part of sec. 8, T. l N., R. 7 E., 
150 feet south of locality 23. Wapanucka formation, lower part. 

3 9. Fine-grained black sandstone, ^ mile south of the NW. cor., sec. 8, T. 

1 N., R. 7 E. Caney shale, upper part. 

41. Limestone, 600 feet south of the NW. cor., sec. 8, T. 1 N., R. 7 E. 
Wapanucka limestone, upper part. 

43. Red limestone, just north of Gibson’s house near center of SW. 54 , sec. 

9, T. 1 N., R. 7 E. Limestone that occurs 15 feet below the Lehigh 
coal of the McAlester formation. 

44. Sandy limestone, bank of Canyon Creek NW. cor., sec. 9, T. l N., R. 7 

E. Savanna formation, lower part. 

45. Sandstone, near center of NW. 54, sec. 9, T. 1 N., R. 7 E. Savanna 

formation, near base. 

46. Limestone, 2,100 feet north and 500 feet east (west central part) of 

sec. 9, T. l N., R. 7 E. Red limestone that at the eastern edge of 
the quadrangle occurs at 15 feet below the Lehigh Coal of the Mc¬ 
Alester formation. 

47. Limestone, in road just north of west central part of sec. 11, T. 1 N., 

R. 7 E. Savanna formation, lower part. 

49. Shale, strip pit, sec. 14, T. 1 N., R. 7 E. Bed that rests on top of the 

Lehigh coal in the McAlester formation. 

50. Limestone, 600 feet south of the strip pit in sec. 14, T. 1 N., R. 7 E. 

Red limestone 15 feet below Lehigh Coal of the McAlester formation. 
5 2. Limestone, in bend of Coal Creek, east central part of sec. 15, T. 1 N., 
R. 7 E. Red limestone that occurs 15 feet below Lehigh Coal of the 
McAlester formation. 

53. Concretionary limestone, 300 feet east'Of center of sec. 23, T. 1 N., R. 

7 E. Caney shale, near middle. 

54. Shale, where creek crosses road in east; central part of sec. 24, T. 1 N., 

R. 7 E. Caney shale, middle portion. (Cephalopods cut by calcite 
veins which carry sphalerite.) ;i 

5 7. Sandstone, east central part of sec. 20., T. 1 N., R. 8 E. Atoka forma¬ 
tion, lower part, i 

58. Calcareous sandstone, in road at NE. cor., sec. 26, T. 1 N., R. 8 E. 
Atoka formation, lower part. 

62. Shale, in road SW. cor., sec. 4, T. 2 N., R. 5 E. Seminole formation, 

upper part. 

63. Concretionary limestone, east of Jackfork Creek, near center of NE. 54, 

sec. 2, T. 2 N., R. 6 E. Caney shale, lower part. 

64. Calcareous shale, 20 feet below Sycamore limestone, near center of NE. 

54 , sec. 2, T. 2 N., R. 6 E. Woodford formation, upper part. 

67. Slate, south Fork of Jackfork Creek, NE. of 54 , sec. 4, T. 2 N., R. 6 E. 


REGISTER OF LOCALITIES 


241 


73. Yellow limestone, 900 feet southwest of cement bridge on Bois d’Arc 

Creek, east central part of sec. 11, T. 2 N., R. 6 E. Sycamore lime¬ 
stone. 

73A. Shale, 300 feet north of branch of Jackfork Creek just below Syca¬ 
more limestone, near center of east line of sec. 12, T. 2 N., R. 6 E. 
Woodford formation, near top. 

74. Calcareous shale, near creek bed 3 00 feet south of locality 73A. Wood¬ 

ford formation, near top. 

7 5. Shale, along road near north east cor., sec. 13, T. 2 N., R. 6 E. Boggy 
formation, upper part. 

76. Sandstone, top of bluff at NE. cor., sec. 23, T. 2 N., R. 6 E. Wewoka 
formation, top of highest stratum. 

7 7. Shale, 500 feet south and 1,000 feet east of center of sec. 15, T. 2 N., 
R. 6 E. Holdenville formation, basal part. This shale rests upon 
the Wewoka sandstone which extends through locality 76. 

78. Shale, near center of SE. sec. 15, T. 2 N., R. 6 E. Francis formation, 

lower port. 

79. Asphaltic conglomerate, asphalt pit, south line of SW. ^4, sec. 20, T. 

2 N., R. 6 E. Holdenville formation. 

80. Shale, south bank of Spring Creek, south central part of sec. 25, T. 2 

N., R. 6 E. Boggy formation, middle part. 

81. Sandstone, bed of small stream 1,000 feet north of the town of Franks. 

Boggy formation, upper part. 

83. Shale, south bank of Spring Creek 1,500 feet east of pump house in sec. 

34, T. 2 N., R. 6 E. Holdenville formation, base. 

84. Conglomerate, NE. cor. sec. 34, T. 2 N., R. 6 E. Wewoka formation, 

upper part. 

85. Shale, south bank of Spring Creek 1,300 feet east of pump house in sec. 

34, T. 2 N., R. 6 E. Holdenville formation, base. The heavy sand¬ 
stone that occurs below this shale bed and which outcrops in Spring 
Creek at the Pump House is thought to be the uppermost bed of the 
Wewoka formation. 

87. Shale, north central part of sec. 3 5, T. 2 N., R. 6 E. Boggy formation, 
upper part. 

91. Shale, south bank of tributary of Bois d’Arc Creek, near center of sec 
17, T. 2 N., R. 7 E. Boggy formation, upper part. 

93. Shale, same as at locality 91 but 1,000 feet northwest of that locality. 

93A. Shale, same as at locality 91 and 93. West bank of Bois d’Arc Creek 

1,000 feet south and 2,000 feet east of the NE. cor., sec. 17, T. 2 N., 
R 7 E. 

94. Limestone, creek bed north central part of sec. 18, T. 2 N., R. 7 E. 

Boggy formation, upper part. 

95. Shale, near center of SE. sec. 23, T. 2 N., R. 7 E. Boggy formation, 

middle portion. 


242 


REGISTER OF LOCALITIES 


96. Shale, SW. cor., sec. 29, T. 2 N., R. 7 E. Boggy formation, middle 

portion. 

97. Sandstone, near center of south line sec. 30, T. 2 N., R. 7 E. Boggy 

formation, middle portion. 

98. Shale, east central part sec. 31, T. 2 N., R. 7 E. Boggy formation, mid¬ 

dle portion. 

100. Shale, in road at house 1,000 feet south of NE. cor., sec. 17, T. 2 N., 
R. 8 E., Boggy formation, middle part. 

105. Limestone, near center of sec. 18, T. 3 N., R. 4 E. Hart limestone, 

member of the Stratford formation. 

106. Limestone, high point at extreme NE. cor., sec. 20, T. 3 N., R. 4 E. 

Hart limestone, member of Stratford formation. 

108. Limestone, near the center of the SE. Y, sec. 31, T. 3 N., R. 4 E. 

Hart limestone, member of the Stratford formation. 

114. Limestone, south central part of sec. 15, T. 3 N., R. 5 E., on elevation 
between two westward flowing tributaries of Rocky Creek. Francis 
formation, DeNay limestone member. 

116. Shale, south bank of small eastward-flowing creek; 1,800 feet north and 
1,000 feet west of the SE. cor., sec. 22 T. 3 N., R. 5 E. Francis for¬ 
mation, basal part. 

119. Sandstone, on east side of narrow, northward-projecting ridge on the 
east side of the main creek in sec. 34, T. 3 N., R. 5 E. Seminole for¬ 
mation, near top. 

124. Shale, shale pit of Ada Brick Company near the southeast corner of 
Ada. Francis formation near base. 

125- Shale, near the center of the SW. sec. 4, T. 3 N., R. 6 E. This 
point is along the foot of the bluff just south of Ada. Francis for¬ 
mation, lower part. 

127. Limestone, SW. cor., sec. 10, T. 3 N., R. 6 E. Homer limestone mem¬ 
ber of the Holdenville formation. 

128. Shale, l,5 50 feet south and 800 feet east of the NW. cor, sec 10, T. 3 

,N, R. 6 E. Seminole formation, upper part. 

129. Shale, in railroad cut 1,000 feet north of south line of sec. 11, T. 3 N., 

R. 6 E. Wewoka formation, upper part. 

130. Shale, center of east line of NE. Ya>, sec. 12, T. 3 N., R. 6 E. Wewoka 

formation, middle part. 

131. Slate, one-fourth mile west of school house in west center of sec. 15, 

T. 3 N., R. 6 E. Woodford formation, upper part. 

132. Sandstone, at top of bluff south of artesian well in center of sec. 16, 

T. 3 N., R. 6 E. 

133. Sandstone, at foot of bluff, south central part of sec. 16, T. 3 N., 

R. 6 E. Boggy formation lower part. (This bed is only a few feet 
above the Caney contact.) 

134. Shale, just above the bed exposed at locality 133 and 300 feet north 

of that point. Boggy formation, lower part. 


REGISTER OF LOCALITIES 


243 


13 5. Red-brown sandstone, on side of bluff east of the artesian well and south 
of Ford’s house in sec. 16 , T. 3 N., R. 6 E. Boggy formation, lower 
part. 

13 6 . Shale, about half way down side of escarpment east of the artesian well 
in the center of sec. 16, T. 3 N., R. 6 E. Boggy formation, lower 
part. 

137. Sandstone, in road cut 500 feet south of NW. cor., sec. 17, T. 3 N. f 

R. 6 E. Seminole formation, upper part. 

138. Shale, south bluff of little creek in the NE. cor., sec. 17, T. 3 N., R. 6 

E. Holdenville formation, basal part. 

139. Shale, at log barn, base of bluff south of Ford’s house in sec. 16, T. 3 

N., R. 6 E. Boggy formation, lower part. 

140. Shale, near the NE. cor., sec. 21 , T. 3 N., R. 6 E. Caney shale, mid¬ 

dle portion. 

141. Shale and limestone concretions, in railroad cut at SW. cor., sec. 22 . 

T. 3 N., R. 6 E. Caney shale, lower part. 

142. Limestone concretion, west side of railroad at NW. cor., sec. 27, T. 

3 N., R. 6 E. Caney shale, base. 

144. Calcareous shale, south side of railroad 1,000 feet east of center of 

sec. 27, T. 3 N., R. 6 E. Caney shale, base. 

145. Slate, 50 feet west of locality 144, but below Sycamore limestone. 

Woodford formation, top. 

146. Slate, in road 1,000 feet north of the SE. cor., sec. 28, T. 3 N., R. 6 E. 

Woodford, lower part. 

148. Slate, in road, south bluff of Jackfork Creek, at NW. cor., sec. 34, T. 

3 N., R. 6 E. Woodford, lower part. 

150. Shale and limestone concretions, bed of Jackfork Creek, north central 

part of sec. 3 5, T. 3 N., R. 6 E. Caney shale, lower part. 

152. Shale, 1,300 feet north and 200 feet east of Love Lady School, in SW. 

cor., sec. 4, T. 3 N., R. 7 E. Wewoka formation, lower part. 

153. Limestone, NE. cor., sec. 6 T. 3 N., R. 7 E. Wekowa formation, upper 

part. 

154. Limestone, near top of high southwestward projecting point at NW. 

cor., sec. 18 , T. 3 N., R. 8 E. Campophyllum-bearing limestone 15 
feet below the top of the Boggy formation. 

155. Shale, near center of NW. 54 , sec. 7, T. 3 N., R. 7 E. Wewoka forma¬ 

tion, middle part. 

1 56. Shale, 1,000 feet south and 2,000 feet east of the NW. cor., sec. 7, 

T. 3 N., R. 7 E. Wewoka formation, middle part. 

1 5 8 . Shale, center of east line sec. 9, T. 3 N., R. 7 E. Senora formation, 
near base. 

159 . Calcareous sandstone, top of escarpment in NW. cor., sec. 11 , T. 3 N., 

R. 7 E. Senora formation, near base. 

160 . Limestone, 2,000 feet north and 1,000 feet east of the SW. cor., sec. 

ll, T. 3 N., R. 7 E. Campophyllum-bearing limestone 15 feet below 
the top of the Boggy formation. 


244 


REGISTER OF LOCALITIES 


161. Shale, side of southward-facing escarpment, center of north line of sec. 

18, T. 3 N., P. 7 E. Wewoka formation, upper part. 

162. Shale, center of sec. 18, T. 3 N., R. 7 E. Boggy formation upper part. 

163. Shale, north central part of sec. 18, T. 3 N., R. 7 E., an area of several 

acres, south of locality 162. Upper Senora and lower Wetumka for¬ 
mations. 

164. Shale, north central part of sec. 19, T. 3 N., R. 7 E. Boggy formation, 

lower part. 

165. Shale, center of east line of SE. 34, sec. 22, T. 3 N., R. 7 E. Boggy 

formation, middle part. 

166. Shale, center of NE. 34 , sec. 22, T. 3 N., R. 7 E. Boggy shale, middle 

part. 

167. Conglomerate, (limestone pebbles) 500 feet south and 800 feet east of 

the center of sec. 23, T. 3 N., R. 7 E. Boggy formation, upper part. 

168. Shale above brown sandstone, east side of Owl Creek, near center of 

SW. 34 , sec. 24, T. 3 N., R. 7 E. Boggy formation, upper part. 

169. Shale, 1,500 feet south and 500 feet east of the NW. cor., sec. 27, T. 

3 N., R. 7 E. Boggy formation, lower part. 

170. Sandy limestone, just north of railroad, NE. cor., sec. 29, T. 3 N., R. 

7 E. Caney shale, upper part. 

17OA. Limestone, NE. cor., sec. 33, T. 3 N., R. 7 E. Wapanucka limestone. 

171. Limestone, 1,500 feet north and 300 feet west of SE. cor., sec. 7, T. 

3 N., R. 8 E. Campophyllum-bearing limestone 15 feet below the top 
of the Boggy formation. 

172. Conglomerate, center of west line of sec. 8, T. 3 N., R. 8 E. Thurman 

sandstone, lower part. 

173. Sandy, conglomeratic limestone, NW. cor., sec. 31, T. 3 N., R. 8 E. 

Boggy formation, middle portion. 

178. Shale, in gully that drains northward from eastern part of town of 
Center, east side of sec. 19, T. 4 N., R. 5 E. 

184. Limestone, in railroad right of way at NE. cor., sec. 8, T. 4 N., R. 6 E. 
Belle City limestone, lower part. 

186. Shale, 750, feet south of NW. cor., sec. 13, T. 4 N., R. 6 E. Seminole 

formation, top. 

187. Shale, north central part sec. 14, T. 4 N., R. 6 E. Francis formation, 

lower part. 

188. Conglomerate, center of east line SW. 34 , sec. 17, T. 4 N., R. 6 E. Ada 

formation lower part. 

191. Black limestone, near center of SE. 34 , sec. 31, T. 4 N., R. 6 E. Ada 

formation, upper part. 

192. Conglomeratic sandstone, west side of asphalt pit in NW. 34 , sec. 31, 

T. 4 N., R. 6 E. 

193. Asphaltic sandstone, asphalt pit, NW. 34 , sec. 31, T. 4 N., R. 6 E. 

195. Shale, center of north line of SE. 34 , sec. 2, T. 4 N., R 7 E. Wewoka 
formation 10 feet below top. 


REGISTER OF LOCALITIES 


245 


196. Shale, 300 feet southwest of locality 195, same horizon. 

197. Limestone, center of north line of NW. 54> sec. 3, T. 4 N., R. 7 E. 

Homer limestone member of Holdenville formation. 

198. Limestone, 800 feet east and 800 feet south of DeNay school, in sec. 

5, T. 4 N., R. 7 E. DeNay limestone member at base of Francis for¬ 

mation. 

199. Shale, southeastern part of NE. >4, sec. 16, T. 4 N., R. 7 E. Wewoka 

formation, upper part. 

199A. Limestone, east central part of SE. J4> sec. 18, T. 4 N., R 7 E. Homer 
limestone member of the Holdenville formation. 

200. Shale, side of escarpment, near center of NE. 54. sec. 30, T. 4 N., R. 

7 E. Holdenville formation, basal bed. 

201. Sandstone, in road cut at top of hill east of Muddy Boggy Creek at SW. 

cor., sec. 29, T. 4 N., R. 7 E. Wewoka formation, upper part. 

202. Shale, center of south line sec. 30, T. 4 N., R. 7 E., 300 feet north of 

graveled road. Holdenville formation, lower part. 

203. Shale, 1,000 feet east and 200 feet south of NE. cor., sec. 5, T. 4 N., 

R. 8 E. Wewoka formation, lower part. 

204. Shale, one half mile north and 800 feet west of the SE. cor., sec. 6, 

T. 4 N., R. 8 E. Wewoka formation, lower part. 

205. Shale, 1,000 feet south of the NW. cor., sec. 6, T. 4 N., R. 8 E. Wewoka 

formation, lower part. 

206. Shale, north bank of Muddy Boggy Creek center of west line of sec. 8, 

T. 4 N., R. 8 E. Wetumka formation, lower part. 

209A. Limestone and 10 feet lower a sandstone, on side of eastward-facing 
bluff, center of east line of SW. 54* sec. 28, T. 5 N., R. 5 E. Vanoss 
formation, middle part. 

210. Sandstone, in road 1,800 feet north of SE. cor., sec. 32, T. 5 N., R. 
5 E. Vanoss formation, middle part. 

214. Shale, in road 500 feet west of center of sec. 24, T. 5 N., R. 6 E. 

Francis formation, middle part. 

215. Sandy limestone, 1,200 feet north of the SE. cor., sec. 12, T. 5 N., R. 

7 E. Holdenville-Wewoka contact. 

216. Limestone, near center of SE. 54* sec. 12, T. 5 N., R. 7 E. Homer 

limestone member of the Holdenville formation. 

216A. Limestone, north bluff of little creek, near center of west line of NE. 
54, sec. 13, T. 5 N., R. 7 E. 

217. Limestone, center of east line of sec. 23, T. 5 N., R. 7 E. Homer 

limestone member of the Holdenville formation. 

218. Shale and limestone concretions, 1,000 feet west of the NE. cor., sec. 

30, T. 5 N., R. 7 E. Francis formation, lower part. 

219. Shale, west side of creek near center of sec. 30, T. 5 N., R. 7 E. Francis 

formation, lower part. 

220. Limestone, near center of north line of sec. 32, T. 5 N., R. 7 E. DeNay 

limestone at base of Francis formation. 


246 


REFERENCES 


221 . Limestone, 500 feet north of center of south line of sec. 33, T. 5 N., 

R. 7 E. Sasakwa limestone member of the Holdenville formation. 

222 . Limestone, top of hill near north line of NE. sec. 3 4, T. 5 N., R. 

7 E. Sasakwa limestone member of the Holdenville formation. 

223. Sandy limestone, near center of west line of sec. 18 , T. 5 N., R. 8 E. 

Wewoka formation, upper part. 

225. Limestone, 1,500 feet east and 700 feet north of the SW., cor., sec. 7, 
T. 6 N., R. 7 E. Belle City limestone, upper part. 

228 . Limestone, in road, 300 feet west of NE. cor., sec. 30, T. 6 N., R. 7 E. 
Francis formation, near top. 

230. Limestone, railroad cut one-fourth mile south of Sasakwa. Sasakwa 

limestone member of the Holdenville formation. 

231. Shale, south center of sec. 10 , T. 6 N., R. 8 E. Holdenville formation, 

basal part. 

232. Shale, just north of railroad bridge north central part of sec. 16 , T. 6 

N., R. 8 E. Holdenville formation, lower part. 


REFERENCES 


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Girty, Geo. H., 

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REFERENCES 


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20 . Lower Carboniferous Species: Geol. Survey of Illinois, vol. 5, 1873. 

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Morningstar, Helen 

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24. Notice of the genus Chonetes as found in the Western States and Ter¬ 

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26. The Carboniferous ammonoids of America: U. S. Geol. Survey, Mon. 

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Smith, S. 

27. The Genus Lonsdaleia and Dibunophyllum Rugosum: Quart. Jour. Geol. 

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29. Paleontology of Illinois: Paleozoic Bryozoa: Geol. Survey of Illinois. 

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30. The Batesville sandstone of Arkansas: (Trans. N. Y. Acad. Sci., vol. 16, 

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31. The Mississippian brachiopodoa of the Mississippi Valley Basin. Geol. 

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33. Fossils from the Carboniferous rocks of the interior States. Contri¬ 

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